STATE OF UTAH DEPARTMENT OF NATURAL RESOURCES

Technical Publication No. 99 GROUND-WATER HYDROLOGY OF OGDEN VALLEY AND SURROUNDING AREA, EASTERN WEBER COUNTY, UTAH, AND SIMULATION OF GROUND-WATER FLOW IN THE VALLEY-FILL AQUIFER SYSTEM

By Charles Avery U.S. Geological Survey

Prepared by the United States Geological Survey in cooperation with the Utah Department of Natural Resources Division of Water Rights 1994

CONTENTS

Abstract 1 Introduction 2 Purpose and scope 3 Methods of investigation...... 3 Previous studies 3 Hydrologic-data site numbering system 4 Acknowledgments 4 Description of study area...... 4 Physiography...... 4 Climate 4 Population, land use, and water supplies.. 6 Hydrogeologic setting 7 Stratigraphy and hydrogeologic units 7 Structure 7 Surface-water hydrology 14 Streams 14 Reservoirs 14 Irrigation and other diversions 20 Water quality 21 Ground-water hydrology of consolidated rocks surrounding Ogden Valley...... 21 Recharge 21 Discharge '" 25 Ground-water hydrology of valley-fill deposits in Ogden Valley...... 27 Recharge '" 27 Movement. 37 Hydraulic characteristics. 37 Storage. 42 Discharge . 42 Effects of Pineview Reservoir 51 Water quality 51 Water budget for the valley-fill aquifer system...... 53 Recharge '" 53 Precipitation 53 Irrigation and irrigation distribution losses 53 Losing streams 57 Pineview Reservoir. 59 Subsurface inflow 59 Discharge 60 Gaining streams 60 Springs and drains...... 61 Wells. 61 Evapotranspiration. 61 Pineview Reservoir 63 Subsurface outflow...... 63 Simulation of ground-water flow in the valley-fill aquifer system 63 Model design and assumptions...... 63 Model boundary conditions 65

iii CONTENTS-Continued

Streams 65 Drains 67 Wells 67 Evapotranspiration 67 Areal recharge 67 Hydraulic properties 67 Hydraulic conductivity 67 Storage coefficient...... 68 Vertical hydraulic conductivity 68 Initial conditions...... 68 Model calibration and simulation 71 Steady-state calibration...... 71 Water levels...... 71 Gains and losses in streams and drains...... 71 Water budget 73 Transient simulation...... 73 Water-level changes 73 Spring Creek drainage 74 Water budget 74 Simulation of hypothetical conditions 75 Drought...... 79 Increased discharge from wells 79 Need for further refinement of the computer simulation...... 81 Summary and conclusions...... 81 References cited...... 82

PLATES

[Plates are in pocket]

1. Map showing geology, precipitation, and selected hydrologic-data sites in Ogden Valley, Utah, and surrounding area 2. Map showing hydrologic-data sites and ground-water quality in Ogden Valley, Utah, 1985

FIGURES

1. Map showing location of the study area 2 2. Diagram showing numbering system used in Utah for hydrologic-data sites. 5 3. Photograph of the Wasatch Range on west side of Ogden Valley near Liberty, Utah 6 4. Photograph of Pineview Reservoir (looking north along the North Fork Ogden River arm of the reservoir) 7 5. Map showing thickness of valley-fill deposits 13 6. Map showing location of sites in Spring Creek drainage where discharge was measured monthly.. 16 7. Hydrograph showing daily mean discharge at Spring Creek at Huntsville (station 10137900), September 1985 through April 1987.... 17 8. Composite hydrograph of discharge determined from monthly measurements at seven sites iII the Spring Creek drainage, November 1984 through June 1986 18

iv FIGURES-Continued

9. Hydrographs of daily mean discharge at the South Fork Ogden River near Huntsville (station 10137500) and at Wheeler Creek near Huntsville (station 10139300), July 1984 through September 1986 19 10. Photograph of Liberty Springs at Liberty, Utah (looking east from hillside on Wasatch Range toward Bear River Range) 27 II. Map showing potentiometric surface of the principal aquifer, June 1985 38 12-19. Hydrographs showing: 12. Water level in wells in the upper South Fork Ogden River valley, 1984-86 39 13. Water level in wells near the Ogden well field and Pineview Reservoir, and stage of Pineview Reservoir, 1984-86 40 14. Water level in wells in the principal aquifer near Pineview Reservoir, 1935-61 43 15. Water level in wells in the principal aquifer near Pineview Reservoir, 1932-84 44 16. Water level in wells in the principal aquifer and stage of Pineview Reservoir, 1984-86 45 17. Water level in wells in the upper South Fork Ogden River valley, 1984-86 46 18. Water level in wells in the North Fork Ogden River valley, 1984-86 47 19. Water level in wells near the North Fork Ogden River channel, 1984-86 48 20. Map showing water-level rise in the principal aquifer from late February to early June 1985 49 21. Hydrographs showing water level in wells in the shallow water-table aquifer, 1970-71 50 22. Graphs showing Ogden well-field pumpage, water level in well (A-6-2)18bad-l, and stage of Pineview Reservoir, July 1984 through July 1986 62 23. Schematic section of the two-layer ground-water flow model simulating the aquifer system in Ogden Valley 64 24-26. Maps showing: 24. Model grid, areal distribution of active cells, and boundary steady-state recharge and discharge for the model of the ground-water system in Ogden Valley...... 66 25. Distribution of hydraulic-conductivity values for layer 2 (principal aquif~r) of computer model for Ogden Valley...... 69 26. Distribution of hydraulic-conductivity values for layer 1 (shallow water-table aquifer) of computer model for Ogden Valley...... 70 27. Graphs showing simulated and measured water-level change for three observation wells in the upper North Fork Ogden River valley, 1985-86 76 28. Graphs showing simulated and measured water-level change for three observation wells in the south part of Ogden Valley, 1985-86 77 29. Map showing simulated water-level change in the principal aquifer, mid-February through May 1985 78 30. Graphs showing water-level change in wells for 1985-86 simulation and for drought simulation 80

TABLES

I. Description of hydrogeologic units...... 8 2. Streamflow characteristics at selected gaging stations 15 3. Mean monthly and mean annual discharge for selected gaging stations 15 4. Miscellaneous measurements of streamflow, specific conductance, and water temperature during base flow in Ogden Valley, February 23 to March I, 1985 22 5. Miscellaneous measurements of streamflow, specific conductance, and water temperature during base flow, upper Middle Fork Ogden River, October 1984, and Wheeler Creek, October 1985 24 6. Records of springs...... 28

v TABLES-Continued

7. Records of wells...... 30 8. Chemical analyses of water samples from wells 54 9. Chemical analyses of water samples from springs 56 10. Water budget for the valley-fill aquifer system, mid-February 1985 through January 1986 58 11. Water level in selected observation wells during February and June 1985 and May 1986 72 12. Simulated water budget for the valley-fill aquifer system, mid-February 1985 through January 1986 74 13. Simulated and measured discharge to Spring Creek...... 79

CONVERSION FACTORS, VERTICAL DATUM, AND ABBREVIATED WATER-QUALITY UNITS

Multiply By To obtain

acre 4,047 square meter 0.004047 square kilometer acre-foot 1,233 cubic meter cubic foot per second 0.02832 cubic meter per second 28.32 liter per second foot 0.3048 meter foot per day 0.3048 meter per day foot squared per day 0.0929 meter squared per day gallon 3.785 liter gallon per minute 0.06308 liter per second inch 25.4 millimeter 2.54 centimeter mile 1.609 kilometer square mile 2.590 square kilometer

Water temperature is given in degrees Celsius (0C), which can be converted to degrees Fahrenheit (oF) by the following equation: OF = 1.8 (0e) + 32.

Air temperature is given in degrees Fahrenheit (OF), which can be converted to degrees Celsius (oC) by the following equation: °C =(OF - 32)11.8.

Sea level: In this report "sea level" refers to the National Geodetic Vertical Datum of 1929-a geodetic datum derived from a general adjustment of the first order level nets of the United States and Canada, formerly called Sea Level Datum of 1929. Chemical concentration is given in milligrams per liter (mg/L) or micrograms per liter (j..lglL). Milligrams per liter expresses the concentration of chemical constituents in solution as weight (milligrams) of solute per unit volume (liter) of water. One thousand micrograms per liter is equivalent to 1 milligram per liter. For concentrations less than 7,000 milligrams per liter, the numerical value is about the same as for concentrations stated in the inch­ pound units of parts per million.

vi GROUND-WATER HYDROLOGY OF OGDEN VALLEY AND SURROUNDING AREA, EASTERN WEBER COUNTY, UTAH, AND SIMULATION OF GROUND-WATER FLOW IN THE VALLEY-FILL AQUIFER SYSTEM

By Charles Avery U.S. Geological Survey

ABSTRACT

The ground-water resources in Ogden Val­ melt and seepage from stream channels are the ley, eastern Weber County, Utah, were the subject major sources of recharge during spring runoff. of a study to provide a better understanding of the During the remainder of the year, subsurface hydrologic system in the valley and to estimate the inflow from bedrock and infiltration of irrigation hydrologic effects of future ground-water develop­ water probably are the major sources of recharge. ment. The study area included the drainage basin Ground-water discharge occurs by seepage to ofthe Ogden River upstream from Pineview Reser­ streams, springs, drains, and Pineview Reservoir; voir dam and the drainage basin ofWheeler Creek. by evapotranspiration; and by pumping from Ogden Valley and the surrounding area are under­ wells. lain by rocks that range in age from Precambrian to Quaternary. Ground-water flow in the principal aquifer is The consolidated rocks that transmit and from the valley margins toward Pineview Reser­ yield the most water in the area surrounding Ogden voir in the southern part of Ogden Valley. Most Valley are the Paleozoic carbonate rocks and the ground-water flow near Pineview Reservoir is Wasatch Formation of Tertiary age. Much of the upward but downward leakage may occur near the recharge to the consolidated rocks is from snow­ Ogden well field. melt that infiltrates the Wasatch Formation, which In general, the dissolved-solids concentra­ underlies a large part of the study area. Discharge tion of water in the valley-fill aquifer system does from the consolidated rocks is by streams, evapo­ not exceed 350 milligrams per liter. Most of the transpiration, springs, subsurface outflow, and water is a calcium bicarbonate type. pumping from wells. Water in the consolidated rocks is a calcium bicarbonate type and has a dis­ A three-dimensional finite-difference com­ solved-solids concentration of less than 250 milli­ puter model of the valley-fill aquifer system was grams per liter. used to simulate ground-water flow. Transmissiv­ The unconsolidated valley-fill deposits, ity values for the principal aquifer estimated from which constitute the valley-fill aquifer system, are the model ranged from 20 to 230,000 feet squared more than 750 feet thick in parts of Ogden Valley. per day. Simulated recharge to the valley-fill aqui­ Water in the northern part of Ogden Valley and fer system determined for the transient simulation along the margins ofthe southern part ofthe valley ranged from 109 to 284 cubic feet per second, and is unconfined; water in the center of the southern simulated discharge ranged from 115 to 209 cubic part ofthe valley is confined in the lower, principal feet per second. The model also was used to sim­ aquifer and unconfined in the overlying shallow ulate the hydrologic effects of a hypothetical 1­ water-table aquifer. Direct infiltration from snow- year drought and increased discharge from wells. 114 0 1'3" 1120 42"'------,- -- --~ - ~- additional municipal water supplies in the valley will I\.( I increase. I \ CACHE\ ,~.~~CHII 1BOX ELDER Land use in Ogden Valley is changing from crop­

I ~:Jtat 0 ~~l. J land and pasture that is irrigated almost entirely by sur­ ~~_ .I~ ~~""".I 0 41oL__ t;.':'_--l10 _ face-water sources and springs to subdivided housing , _~ SUMM~_ roA(~GET1-1 I Sa~~ ke City --...,~ --'I. '1 tracts that primarily use individual or small community lSAL~ ~('- 11-/- I UINTAH ' I ILAK';r'/"jASAlCH1 I wells. Hydrologic changes that result from the changes I t...... ,I, I I in land use may affect the quantity and quality of ~ L_'""~---~,d~;~-\J ,",""" ! i ground water. I l. L..;---,----'------,. I The increased use of ground water in Ogden Val­ JUAB (- r" CARBON f I ley and the potential effects of land-use changes on 1I ------lir-) i \------t-----1 water quantity and quality is of concern to local water I MILLARD I SANPETE I EMERY r GRAND I users, developers, and the State of Utah. In addition, 39' 1- /)------1 { -I, 'I ' downstream users are concerned that increased ground­ ~------.L;./___--,,-_-.lSEVIER' ----J\.---1_ water withdrawals may reduce streamflow. To address I BEAVER \'\ PIUTE r \. I these concerns, the U.S. Geological Survey, in cooper­ ~------~---'----WAY~~----; 38" j ation with the Utah Department of Natural Resources, I IRON'--: GARFIELD r( I Division of Water Rights, studied the ground-water I r' ,I resources of Ogden Valley from July 1984 to June ---LL.._.,-J--L------J) SAN JUAN I 1987. The purpose ofthe study was to provide a better tWASHINGTON I KANE,} I I' , understanding of the hydrologic system in Ogden Val­ 3JO Iol.....- __ ----J..jI ... _ ----d:..lj ...l.- _- .--II ley and to estimate the hydrologic effects of future

o 20 40 60 MILES ground-water development. 6 2'0 40 60 KILOMETERS Most usable ground water in Ogden Valley EXPlANATION comes from aquifers in the unconsolidated valley-fill ~ STUDYAREA deposits. The valley-fill deposits in Ogden Valley extend about IS miles in length, I to 4 miles in width, Figure 1. Location of the study area. and trend in a northwest-southeast direction. The series of aquifers and confining units of the unconsolidated valley-fill deposits are referred to as the valley-fill aqui­ fer system in this report. Ground water in Ogden Valley has been consid­ ered fully appropriated for many years. Additional INTRODUCTION water development in the area could be accomplished through a transfer based on an existing irrigation-water Since about 1915, Ogden, Utah (fig. 1), which right or through an exchange of surface-water rights for had a population of 64,907 in 1980 (Bureau of the Cen­ water in Pineview Reservoir, which stores water for sus, 1982), has obtained most of its municipal water irrigation, municipal supply, hydroelectric-power gen­ supply from Ogden Valley in eastern Weber County, eration, and flood control. Surface-water rights are northern Utah (pI. 1). At present (1987), Ogden obtains leased from the Weber Basin Conservancy District. most of its municipal water supply from ground water The majority of surface-water-right exchanges are for from a well field in Ogden Valley and from surface domestic use although some large users recently have filed exchange applications. Through the surface­ water from Pineview Reservoir and Wheeler Creek (pI. water-right exchange application program, the quantity 2). Because the population of Ogden has decreased ofwater that will be pumped by the new well is released nearly 10 percent since 1960, additional municipal from Pineview Reservoir. The surface-water-right water supplies probably will not be needed in the near exchange application program assures an adequate sup­ future. In contrast, the population in Ogden Valley has ply of water for downstream users. Downstream increased steadily, especially in the last few years, and demands on Ogden River water include irrigation, probably will continue to increase. Thus, the need for municipal supply, and hydroelectric-power generation.

2 Purpose and Scope ing October 1984 and on Wheeler Creek during Octo­ ber 1985. Flow measurements were made on several This report describes the results ofthe hydrologic irrigation ditches during the summer of 1985. Water study of Ogden Valley and the surrounding area. samples from 23 wells, 5 springs, and 2 minor seeps Hydrologic data collected during the study and selected were collected to analyze the quality of ground water. data from previous studies were used to interpret the A three-dimensional, finite-difference digital­ ground-water hydrology of the study area. These data computer model was used to simulate ground-water were also used to develop a digital-computer model to flow in the valley-fill aquifer system of Ogden Valley. simulate ground-water flow in the aquifer system of The model was used to evaluate the adequacy of avail­ Ogden Valley. able data in simulating ground-water flow in Ogden The report describes hydrologic conditions in Valley. Hydrologic effects of a hypothetical drought Ogden Valley in terms of ground-water recharge, and of increased withdrawals from wells also were sim­ movement, and discharge; surface-water and ground­ ulated. water relations; ground-water storage; and general water quality. A water budget for 1985 was prepared Previous Studies from data collected during 1985 and from other infor­ mation. Available data were evaluated in the context of Fortier (1897) made discharge measurements of understanding and analyzing changes to the hydrologic the Ogden River, its major tributaries, and irrigation use system. to resolve a water-rights dispute between irrigators in Ogden Valley and irrigators near Ogden. From July to Methods of Investigation September, increasingly more surface water flowed out of the valley than flowed into it; the discrepancy was Most of the detailed hydrologic data for this attributed to seepage from irrigated lands that had been study were collected from August 1984 to July 1986. returned to surface water. Additional data from other sources also are included in Browning (1925) analyzed a series of surface­ this report. Electrical resistivity soundings were made water discharge measurements made on the Ogden throughout Ogden Valley to estimate the thickness of River system during the summers of 1921 and 1925. alluvial deposits. Major springs and wells in Ogden Numerous gaining and losing reaches in the river sys­ Valley and the surrounding area, including all public­ tem were detected and related to the hydraulic connec­ supply and other large-yield wells, were inventoried. tion between river and aquifer. Browning (1925) Water levels in 21 wells were measured monthly indicated that withdrawals from the now-abandoned (except for biweekly measurements in April 1985) for Ogden artesian well field may have had some effect on a 2-year period. Also, water levels in a large number of streamflow depletion. wells were measured in February and June 1985 and in June 1986. A 4-day aquifer test was conducted on 7 The first comprehensive study of ground-water observation wells in the city of Ogden well field. Sin­ resources for Ogden Valley was conducted by Leggette gle-well, I-hour aquifer tests were conducted on 5 and Taylor (1937). Leggette and Taylor (1937) investi­ domestic wells. gated the ground-water hydrology near the Ogden arte­ sian well field before the existence of Pineview Measurements were made of water discharging Reservoir. from the valley-fill deposits into Pineview Reservoir. Open-ended barrels that had a collection port on the Thomas (1945, 1952, 1963) used water-level data closed end (seepage meters) were driven into the bot­ to identify sources ofrecharge to the artesian aquifer in tom ofthe reservoir, and the volumes of water collected the valley-fill deposits that supplies the Ogden artesian over time were measured. Data obtained were used to well field. He also determined a tentative water budget calculate the estimated total discharge. for the aquifer (Thomas, 1963). Surface-water and water-quality data also were Lofgren (1955) described the vaHey-fill deposits collected. Streamflow measurements were made dur­ in Ogden Valley. Some inferences were made as to the ing February 1985 on major streams, except for the hydrologic characteristics of the various deposits. South Fork Ogden River. Streamflow measurements The most recent hydrologic study in Ogden Val­ were made on the upper Middle Fork Ogden River dur- ley was conducted by Doyuran (1972). Water-quality

3 sampling indicated coliform counts that locally major tributaries of the Ogden River-the North Fork, exceeded standards and iron bacteria in water that dis­ Middle Fork, and South Fork-flow from the upland charged from artesian wells. Vegetation distribution areas surrounding Ogden Valley into Pineview Reser­ was mapped, and vegetative evapotranspiration was voir (pI. 1). estimated. High mountains border Ogden Valley except on the north and south where lower hills form divides Hydrologic-Data Site Numbering System between the Ogden River and adjacent drainages. The altitude of the southeastern part of the valley is about The hydrologic-data site numbering system used 4,900 feet. The altitude increases to about 5,000 feet at in Utah is shown in figure 2. Surface-water gaging sta­ the North Fork Ogden River at Eden and to about 5,100 tions that have continuous discharge records available feet at the canyon mouths of Middle Fork Ogden River are identified by an eight-digit downstream-order num­ and South Fork Ogden River. The altitude of the north­ ber adopted by the U.S. Geological Survey. For exam­ ern part ofthe valley near Eden is about 5,100 feet. The ple, the gaging station on the South Fork Ogden River altitude increases to about 5,600 feet in the upper North near Huntsville, Utah, is designated 10137500. Fork Ogden River drainage, north of Liberty. The mountains surrounding Ogden Valley are more than Acknowledgments 3,000 feet above the valley floor (fig. 3). About 15 per­ cent of the study area is above 8,000 feet (Haws and The author gratefully acknowledges the coopera­ others, 1970, fig. 4). Willard Peak, northwest ofOgden tion given by Gary Clark and the Ogden City Water Valley, is the highest point in the study area and has an Utilities during the 4-day aquifer test. Thanks also are altitude of 9,764 feet. expressed to those persons who permitted access to their property and water wells in order to accomplish Climate the necessary data collection. Climatic records have been collected at the site of DESCRIPTION OF STUDY AREA Pineview Reservoir dam since 1935. Average annual precipitation at the station for 1951-80 was 28.79 The study area consists of the drainage basin of inches (U.S. National Oceanic and Atmospheric the Ogden River upstream from the dam at Pineview Administration, 1982). Annual precipitation for 1935­ Reservoir, which was completed in 1936, and the drain­ 1986 ranged from 17.09 inches in 1966 to 53.45 inches age basin of Wheeler Creek, which flows into the in 1983. The climate at Pineview Reservoir dam is Ogden River just downstream from the Pineview Res­ affected by orographic features of Ogden Canyon. ervoir dam. The drainage area of the Ogden River upstream from Pineview Reservoir dam is 310 square Two other stations recently have been established miles; the drainage area of Wheeler Creek is 11.1 to record climatic data. One station is at Huntsville square miles. Downstream from Pineview Reservoir Monastery in the southeastern part of Ogden Valley, dam, the Ogden River flows through Ogden Canyon to and the other is at Snow Basin in the mountains of the the Great Salt Lake, west of Ogden, Utah. southwestern part ofthe study area. Sufficient record is not available to establish long-term climatic values at these stations; however, the average annual precipita­ Physiography tion at Pineview Reservoir dam for 1977-85 was 11.9 inches greater than that at Huntsville Monastery. The study area is in the Middle Rocky Mountains Physiographic Province (Fenneman, 1931), which is The estimated distribution of normal (1931-60) characterized mainly by anticlinal mountain ranges and annual precipitation ranges from about 20 inches near intermontane basins. The Wasatch Range borders the Huntsville and the low hills to the south to about 40 west side ofOgden Valley, and the Bear River Range, a inches near the high mountains on the west side of the subdivision of the Wasatch Range, borders the north­ study area (U.S. Weather Bureau, 1963). The average east side of Ogden Valley. Ogden Valley is in the low annual precipitation in the Ogden River drainage above western part ofthe study area. Pineview Reservoir is in Pineview Reservoir dam is about 20.5 billion cubic feet the southern part of Ogden Valley and is a control for based on the U.S. Weather Bureau (1963) precipitation surface-water discharge from the valley. The three distribution. The Wheeler Creek drainage receives an

4 Figure 3. Wasatch Range on west side of Ogden Valley near Liberty, Utah. Willard Peak is indicated by arrow in right background.

average annual precipitation ofabout 784 million cubic housing tracts. The study area is a popular year-round feet. recreational area. Three ski resorts are located in the Precipitation for October to April occurs mainly mountains bordering the valley, game-hunting occurs in the form of snow and accounts for about 75 percent in the surrounding foothills and mountains, and a pop­ of the normal annual precipitation. Most of the snow­ ular boating and beach area exists at Pineview Reser­ melt in Ogden Valley occurs from late March to early voir (fig. 4). April. Snowmelt in the surrounding area usually occurs from April through May, although the snow on the The towns of Huntsville, Eden, and Liberty each south-and southwest-facing slopes usually melts have municipal water systems that are supplied by slightly earlier because ofincreasing radiation from the springs. Eden also has a well that provides supplemen­ sun during the latter part of the winter. tal water, generally during the summer. The Eden and Potential evapotranspiration from a vegetative Liberty water systems supply water to much ofthe pop­ surface that has unlimited soil water can be estimated ulation in the valley north of Pineview Reservoir. from the average annual evaporation from a free-water Agriculture, in the form of stockraising, dairy surface. Free-water surface evaporation for the study operations, and crop farming (mostly irrigated), is the area ranges from slightly less than 35 inches per year to about 40 inches per year (Farnsworth and others, 1982, major form of employment although it is declining in map 3). importance. Of the 16 dairies that are active in Ogden Valley (Utah Department of Agriculture, written com­ Population, Land Use, and Water Supplies mun., 1984),6 are supplied by municipal water sys­ tems, 5 are self-supplied by wells, and the remaining 5 The population of Ogden Valley in 1980 was are self-supplied primarily from springs. Few wells are 3,294 (Bureau ofthe Census, 1982). The population of used exclusively for stock water because surface water the valley has more than doubled since 1960, while the in ditches and canals provides water to most of the live­ population of Huntsville, the only census-designated stock. Although some small areas of cropland and pas­ incorporated town, has remained fairly stable. ture are irrigated by water from wells, most areas are The major land uses in Ogden Valley are crop­ irrigated by water diverted from surface-water sources land and pasture but land use is changing to subdivided and springs.

6 Figure 4. Pineview Reservoir (looking north along the North Fork Ogden River arm of the reservoir). Ogden well field is indicated by arrow on promontory on right side of photograph.

Hydrogeologic Setting Cambrian age, and metasedimentary rocks of Precam­ brian age. Ogden Valley and the surrounding area are On the basis ofdrillers' logs and a resistivity sur­ underlain by rocks that range in age from Precambrian vey, the valley-fill deposits in Ogden Valley are esti­ to Quaternary although Mesozoic rocks are not found in mated to be greater than 500 feet thick at Liberty and the area (table 1). The Precambrian rocks are mainly greater than 750 feet thick northeast ofHuntsville, Utah metasedimentary. Carbonate rocks predominate in the (fig. 5). A gravity survey by Stewart (1958) indicates Paleozoic sequence, whereas deposits of Cenozoic age that the Wasatch Formation, Norwood Tuff, and valley­ are predominately alluvial in origin. At its highest fill deposits in Ogden Valley may be as much as 5,000 stage of about 5,090 feet, Pleistocene Lake Bonneville feet thick. extended into Ogden Valley through Ogden Canyon. Unconsolidated lacustrine sediments undoubtedly were Structure deposited in the valley, but stratigraphic correlation to other Lake Bonneville deposits was not attempted. Ogden Valley is a graben having west-and east­ bounding faults oriented in a northwest-southeast direction. Along the faults, fairly permeable alluvium Stratigraphy and Hydrogeologic Units commonly is displaced against less permeable metasedimentary rocks or Norwood Tuff. Stewart Rocks in the stratigraphic section were grouped (1958) determined that displacement on the western into six hydrogeologic units (table 1) based on rela­ fault zone of Ogden Valley was 2,000 feet, and dis­ tively uniform lithology, similarity in values ofprimary placement on the eastern fault zone was 1,800 feet. A permeability, and types and values ofsecondary perme­ branch of the western fault zone may displace the near­ ability. The hydrogeologic units are the valley-fill surface sediments, now under Pineview Reservoir, by deposits of Quaternary age (including fluvial, slope­ about 25 feet as shown on a cross section interpreted wash, and fanglomerate deposits), Norwood Tuff of from well logs (Thomas, 1945, fig. 2). Stewart (1958) Tertiary age, Wasatch Formation of Tertiary age, car­ mapped another possible buried fault parallel to the bonate rocks of Paleozoic age, clastic rocks of lower western-bounding fault.

7 Table 1. Description of hydrogeologic units

Hydrogeologic units: The codes shown with unit names are used to identify hydrogeologic units, formations, or other deposits in plate I and in tables 6,7, 8, and 9. General lithology and thickness: Descriptions modified from Lofgren (1955), Mullens (\969), Crittenden (1972), Sorensen and Crittenden (1979), Crittenden and Sorensen (\ 985a, 1985b), and Davis (\ 985).

E Hydro­ CI> E til Formation or deposit General lithology and thickness Water-bearing ..c: CI> CI> 1 ';: characteristics geologic -...ell "i CI> unit W en en

Fluvial deposits Poorly sorted, unconsolidated silt, sand, gravel, Low to moderate permeability. (lIIALVM) and cobbles in flood plains and terraces as much Q) l::: as 160 feet above river level. Thickness as much Q) o as 20 feet. oS ]!'" Siopewash and fanglomerate QUarlzite cobbles, boulders, and gravel derived l1. Low to moderate permeability. 'tl (lIIALVM) primarily from erosion of the Wasatch l::: III Formation. Thickness as much as IDO feet. Q) l::: Q) o o Valley-fill deposits Brownish-tan, well-sorted, unconsolidated sand Moderate permeability. 15 (lIIALVM) and silt; gravel and cobbles along the major :I: stream channel. Thickness as much as 150 feet.

CU Valley-fill deposits Interbedded cobbles, gravel, sand, silt, and clay. Moderate to high permeability. l::: cu (l12ALVM) A dark-blue and variegated, micaceous, silty Major water-yielding unit in Ogden o :v>- ...o clay layer (as much as IDO feet thick) exists Valley. Well yields of more than ...l::: "Qj'" throughout the lower valley. Probable thickness I,DOO gallons per minute possible. ~ a: as much as 500 feet. o ;, o 0 N o Q) Z l::: Q) Valley-fill deposits Interbedded gravel, sand, silt, and clay. This Moderate to high permeability. w o o ~ (Il2ALVM) deposit likely occurs in deep parts of the 'Qj structural trough. Probable thickness as much as a: 250 feet. .2 a:

'tlQ) l:::l::: IlI cu Norwood Tuff White to tan-weathering, fine- to medium­ Very low to low permeability. CUo l:::o (I 23NRWD) bedded, friable tuff and sandy tuff. Maximum CUO! Small-yield wells pump from this 0,- thickness may exceed 1,200 feet. unit but drawdowns are large. w0-O 4»4; e.~ e.o :::l-

'tl l:::'" Wasatch Formation and Evanston Light reddish-brown, poorly sorted, Low to moderate permeability. Ill;' (?) Formation (undivided) unconsolidated to poorly consolidated CUcu-0 Major recharge medium for the l:::o (I 24WSTC) sandstone and pebble, cobble, and boulder CUIll upper drainage. Confined unit with 0'" OCU conglomerate. Matrix is gravel, sand, and silt. low artesian pressure. -(Jcu'" Interbeds of sandy siltstone. Basal, brownish­ Ill ... l1.cu gray, conglomeratic sandstone, conglomerate -e. CUe. and gray siltstone. Thickness as much a~ 3,DOO ~:::l o~ feet. 0('0, w~

8 Table 1. Description of hydrogeologic units-Continued

E CIl Formation or deposit General lithology and thickness Water-beari ng Hydro­ s:. :l 1 'C characteristics geologic E CIl unit w en

Park City Formation Franson Member-Interbedded chert, Probably low permeability limestone, sandstone, and sparse phosphate rock resulting from bedding partings, in upper part; light- to medium-gray, cherty fractures, and voids developed limestone and dolomite in lower part. Thickness from solution of bicarbonate from about 400 feet. the rock. Large springs in the Grandeur Member-Dark-gray, fetid limestone eastern part of the study area and dolomite; basal, light-gray limestone. originate from this unit. Thickness 250 to 280 feet.

Phosphoria Formation Meade Peak Member-Dark-gray, phosphatic limestone, dolomite, siltstone, and pelletal phosphorite. Thickness 230 feet.

Wells Formation Light-gray to grayish-orange sandstone. Minor light-gray limestone and dolomite in upper part. Thickness 400 feet. Medium- to light-gray, c: III granular dolomite and medium-dark-gray '2 III limestone in lower part. Thickness 200 feet. > >. UI c: c: Round Valley Limestone Gray, cherty limestone and pale-red siltstone. o :. Thin beds of gray to green limestone in upper o part; gray, cherty limestone in lower part. ~ w Thickness 250 to 300 feet. oJ ~

Humbug Formation Tan and gray siltstone and fine-grained (33IHMBG) sandstone with interbedded dark- to medium­ gray limestone and dolomite. Thickness about 1,600 feet. c: III "Q. Lodgepole Limestone Dark-gray limestone; medium-gray dolomite at Q. 'iii (337LDGP) top. Thickness 900 feet. UI "iii UI :E Deseret Limestone Dark- to light-gray, medium- to thin-bedded limestone and dolomite with thin beds of dark gray to black chert. Thickness 200 to 250 feet.

Gardison Limestone Medium- to dark-gray, thick-bedded to massive dolomite in upper part; dark-gray to black, thin­ to medium-bedded dolomite in lower part. Thickness 295 to 850 feet.

c: Beirdneau Sandstone Tall-, orange-, and brown-weathering. fine- to III '2 medium-grained sandstone. dolomitic o > sandstone, and dolomite. Thickness 250 to 300 oQI feet.

9 Table 1. Description of hydrogeologic units-Continued

IE IV III General lithology and thickness Hydro­ J: CIl Formation or deposit Water-bearing .~ 1 III ";: characteristics geologic 1- CIl LU en unit

Hyrum Dolomite Dark-gray to black, thin- to thick-bedded, fine­ grained dolomite with lenses ofintraformational c: dolomitic breccia. Thickness about 350 feet. .!!! c: o > Water Canyon Formation CD Medium- to dark-gray dolomite in upper part; C medium-gray dolomitic sandstone in lower part. Thickness about 80 feet.

c: .!!! 5 Fish Haven Dolomite Dark- to brownish-gray, very fine to fine­ iii grained dolomite; sparse beds of very light gray dolomite. Thickness 520 to 650 feet. and c: l'll - Laketown Dolomite ....~ 8. (undivided) 0.0 ;:)'0 o o <5 N o Garden City Formation Light-gray, medium- to thick-bedded limestone, W ..J dolomite, and dolomitic limestone with ~ interbedded siltstone or intraformational conglomerate. Thickness about 350 feet.

St. Charles Limestone Dark-gray, white-weathering, thin- to thick­ c: (37ISCRL) bedded dolomite with basal, gray-brown­ l'll '': weathering quartzite. Thickness 450 to 700 feet. ..c E ol'll a; Nouman Dolomite Light-gray, thin- to thick-bedded, finely 0. 0. crystalline dolomite with interbedded gray ::::l limestone in upper part. Thickness 450 to 650 feet.

Bloomington Formation Tan to drab-olive, thin-bedded shale. Interbedded, gray to orange-brown limestone in upper part. Thickness 165 feet. Light- to dark­ gray limestone in middle part. Thickness 500 feet. Tan and olive shale with some interbedded gray limestone in lower part. Thickness 300 feet.

Maxfield Limestone Medium to dark-gray, thin-bedded limestone with drab-olive to greenish-brown, micaceous shale interbedded with gray limestone in middle part. Thickness 850 feet.

10 Table 1. Description of hydrogeologic units-Continued

E Gl III Formation or deposit General lithology and thickness Water-bearing Hydro­ ~ Gl 1 ';:: characteristics geologic 16 Gl w.. en unit

Blacksmith Limestone Gray- to blue-gray, thin- to medium-bedded limestone and dolomite. Thickness about 1,200('1) feet.

Ute Limestone Light- to dark-gray, medium- to thin-bedded c silty limestone with interbedded gray sandstone .!!! and greenish shale. Thickness 700(?) feet. ii E l'll () Gl is Langston Dolomite Brown-weathering, thin-bedded, massive 'C dolomite. Thickness 170 feet. :\j

() (5 oN Ophir Formation Light blue-gray limestone and shaly limestone. W ..J Drab-olive shale in upper part, blue-gray ~ limestone and tan to orange-brown limestone in middle part; light-brown to drab-olive, micaceous shale and brown-weathering sandstone and dolomite in lower part. Thickness 450 to 600 feet.

Tintic Quartzite White, pink, buff, and tan, medium- to thick­ Probably very low permeability. (374TNTC) bedded, medium- to coarse-grained quartzite; Most water movement is through C interbeds of quartz-pebble conglomerate. fractures. l'll ';: Thickness I, I00 to 1,400 feet. J:I E l'll () ~ o Geertsen Canyon White, gray, pink, and light-green, medium- to ..J Quartzite coarse-grained quartzite in upper part; tan, white, maroon, and green quartzite in lower part. Thickness 4,000 to 4,400 feet.

Browns Hole White to terra cotta, well-sorted, medium- to Probably very low permeability. Formation fine-grained quartzite with gray-weathering, Most water movement is through 0.. e::J dense basalt and reworked volcanic fractures. One well in the Mutual o conglomerate in lower part. Thickness about Formation flows at a high rate. E 400 feet. l'll z .r:: OJ « c Mutual Formation Grayish-red, pink, maroon, and pale-purplish, ii: 05 III (400MUTL) medium- to coarse-grained quartzite. Thickness ::::E « 435 to 1,200 feet. () w a: Q. Inkom Formation Purple and drab-olive-green, thin-bedded siltstone, sandstone, argillite, and quartzite with gray-weathering, basal tuff. Thickness 360 to 450 feet.

11 Table 1. Description of hydrogeologic units-Continued

E Hydro­ Ql Formation or deposit General lithology and thickness Water-bearing .c characteristics1 geologic (;j unit w..

Caddy Canyon Quartzite White, tan, gray, green, and purple, medium~ grained quartzite. Thickness 1,500 to 2,500 feet.

Kelley Canyon Formation Dark~gray to black argillite. Locally, drab~ olive siltstone and thin quartzite at top, pinkish~ gray limestone in middle, and gray~weathering dolomite at base. Thickness 2,000 feet.

z Light~green greenish~gray, oct: Maple Canyon Formation to arkosic quartzite ii: and sandstone. Conglomeratic quartzite and lD drab~olive drab~olive :i: argillite in upper part, oct: argillite in lower part, and, locally, basal gray () W limestone. Thickness about 1,500 feet. II: 0. Formation of Perry Canyon Upper member-Medium~ to dark~gray, medium~ to fine~grained, graywacke and gray to dark~green, micaceous siltstone. Thickness about 1,400 feet. Lower member-Gray to black diamictite consisting ofpebble~ to boulder~sized, quartzitic and granitic clasts in black, medium~ to fine~ grained, sandy matrix. Thickness as much as 350 feet.

Formation of Facer Creek Green, purple, and black slate and phyllite. Thickness unknown.

1 The ranges of permeability are defined in terms of hydraulic conductivity as follows: Range Hydraulic conductivity, in feet per day

Very low Less than 0.5 Low 0.5 to 5 Moderate 5 to 50 High 50 to 500 Very high Greater than 500

12 111°52'30" EXPlANATION I --250 -- Line of equal thickness of valley-fill deposits, in feet ­ Interval 250 feet

...... Contact of valley-fill deposits and consolidated rock

R.1W. R. 1 E.

R. 1 E. R.2 E. Base from U.S. Geological Survey Ogden. 1:100.000. 1976

o 2 3 MILES I I I o 2 3 KILOMETERS

Figure 5. Thickness of valley-fill deposits.

13 A previously unmapped fault in the valley-fill ing station that measures discharge into Ogden Valley. deposits was determined from results of an aquifer test Wheeler Creek (pI. 1), which also has an active (1986) conducted at the Ogden well field. The fault was pro­ gaging station, discharges to the Ogden River below jected across the southwest side ofOgden Valley, under Pineview Reservoir dam; thus, it is not part of the Pineview Reservoir, and across the narrow promonto­ inflow to Ogden Valley. ries jutting into the reservoir (pI. 1). Streamflow characteristics at selected gaging sta­ A large syncline extends into Ogden Valley tions are shown in table 2. The South Fork Ogden from south of the study area. The syncline probably is River has the largest drainage area and discharge of all the area within which the Tertiary sediments were of the streams in the study area. Mean monthly and deposited in Ogden Valley (Eardley, 1944, p. 856). The mean annual discharge for the period of record, exclud­ syncline predates the normal faulting that formed ing water years 1982-86, for selected gaging stations is Ogden Valley. shown in table 3. Water years 1982-86 were excluded A series of stacked overthrust plates, including because runoff in those years was greater than the mean the Willard thrust sheet, is exposed in the western part flow. of the study area (Davis, 1985). The structure of the The streams and the valley-fill aquifer system are overthrust plate is very complex and is not fully under­ hydraulically connected and exchange water. Many of stood. Precambrian rocks generally have been thrust the streams lose water and recharge the valley-fill aqui­ over Paleozoic rocks. The overthrusting is considered fer system where the streams flow into Ogden Valley. to predate the deposition of the Wasatch Formation. The North Fork Ogden River, Middle Fork Ogden The structure in the remainder ofthe study area is River, and South Fork Ogden River gain flow from the exposed through erosional windows in the relatively valley-fill aquifer system before entering Pineview Ilat-Iying Wasatch Formation and consists of folds and Reservoir. minor fault features. The Wasatch Formation blankets Water that discharges to Spring Creek, which much of the study area east and south of Ogden Valley. drains much of the area in the valley north and east of Huntsville (fig. 6), originates in the mountains north­ SURFACE-WATER HYDROLOGY east of Huntsville. Flow at the mouth of Spring Creek is perennial (fig. 7) because the creek gains water that Surface water and ground water are hydraulically discharges from the valley-fill deposits east of Hunts­ connected in Ogden Valley. Surface-water data and ville. Discharge at seven sites (fig. 6) in the Spring field observations were used in the analysis of ground­ Creek drainage was measured monthly during Novem­ water flow in the valley-fill aquifer system. ber 1984 through June 1986 and plotted in a composite hydrograph (fig. 8). Streams Discharge at the South Fork Ogden River and at Wheeler Creek during 1984-86 is shown in figure 9. The major streams in the study area are the North The South Fork Ogden River is regulated partly by Fork Ogden River, Middle Fork Ogden River, and Causey Reservoir. Flow in Wheeler Creek generally is South Fork Ogden River. Their juncture to form the characteristic of flow from a small unregulated stream. Ogden River is in the area now inundated by Pineview Reservoir. Other streams that originate in the surround­ Reservoirs ing mountains and that have substantial discharge are WolfCreek, Geertsen Canyon creek, and Bennett Creek Two major reservoirs store surface water in the (pI. I). The remaining streams have smaller watersheds study area. Pineview Reservoir on the Ogden River in and are ephemeral; flow from these streams into Ogden the southwestern part of Ogden Valley provides irriga­ Valley generally occurs only from February through tion and municipal water to the Ogden area, powers a June. small hydroelectric-power-generation plant down­ Locations of selected active (1986) and discon­ stream, and provides a recreational area in Ogden Val­ tinued gaging stations in the study area are shown on ley. Filling of the reservoir began in November 1936, plate 2. Station 10137500 (pI. 2), which is on the South and maximum storage capacity was reached in June Fork Ogden River just upstream from Ogden Valley 1938. The altitude of the full reservoir pool was 4,871 and a major irrigation diversion, is the only active gag- feet. The reservoir had a storage capacity of about

14 Table 2. Streamflow characteristics at selected gaging stations

Discharge Station name and number Period of Drainage (cubic feet per second) record area Maximum Minimum Average (water years) (square miles)

South Fork Ogden River near Huntsville, Utah (]()]J7500) 1921-86 148.0 1,890 9 118

South Fork Ogden River at Huntsville, Utah (10137600) 1960-65 170.0 1,090 3.2 77.8

North Fork Ogden River near Eden, Utah (10137680) 1964-74 6.0 156 .8 12.1

North Fork Ogden River near Huntsville, Utah (10137700) 1960-65 61.4 693 0 35.3

Middle Fork Ogden River above irrigation di versions near Huntsville, Utab (10137780) 1964-74 31.3 744 .4 31.8

Middle Fork Ogden River at Huntsville, Utah (10137800) 1958-65 32.0 623 0 20.1

Spring Creek at Huntsville, Utah (10137900) 1958-65 7.2 210 2.6 IDA and 1986

Wheeler Creek near Huntsville, Utah (10139300) 1959-86 11.1 t600 0 211.2

I Estimated.

2 Streamflow records since 1977 do not include di versions by the city of Ogden.

Table 3. Mean monthly and mean annual discharge for selected gaging stations

Mean monthly discharge (in cubic feet per second) Station Water Mean number years Oct Nov Dec Jan Feb Mar Apr May June July Aug Sept annual discharge

10137500 1922-65 40.2 40.8 42.3 41.3 47.3 797 287 428 144 56.6 42.3 39.1 107 10137500 1966-81 45.3 40.1 39.9 44.4 50.5 97.6 257 446 185 92.2 84.8 60.0 120 10137600 1960-65 7.45 10.8 26.2 26.7 52.8 61.5 259 362 89.5 19.0 10.4 7.66 77.8 10137680 1964-74 388 4.59 4.35 5.53 4.90 11.0 28.7 43.1 22.8 7.87 4.39 3.60 12.1 10137700 1960-65 .03 .03 6.64 16.2 25.2 28.4 149 151 49.5 5.08 1.27 1.83 36.2 10137780 1964-74 2.89 4.14 5.82 8.50 9.90 31.9 100 173 35.9 4.78 1.67 1.78 31.7 10137800 1958-65 20 .28 2.37 1.83 7.50 11.2 97.3 115 14.3 1.08 .17 .50 21.0 10137900 1958-65 6.15 7.21 7.89 6.96 9.40 10.9 13.0 14.6 16.2 9.26 6.81 6.94 9.62 10139300 1959-81 1.34 1.38 1.78 2.65 2.30 7.39 23.6 34.2 26.6 7.10 2.71 1.72 9.40

15 ... 111"45' 11130' en I

41

T. 6 N.

*,.4"Ir.V EXPlANATION

R.2 E. Approximate surface-water drainage divide Base from U.S. Geological Survey Browns Hole, L24,OOO 1964, photorevised 1975 Monthly discharge-measurement site ­ Huntsville, L24,OOO 1955, photorevised 1975 Number is site identification number Snowbasin. L24,OOO 1955, photorevised 1975 "1

Figure 6. Location of sites in Spring Creek drainage where discharge was measured monthly. 200

100 0z 0 () w (f) a: w a.. I- w W LL g co ::J () Z w <.9 a: « I () (f) 10 0 z « w ~ ~ « 0

2 SEPT OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN FEB MAR APR 1985 1986 1987

-...j Figure 7. Daily mean discharge at Spring Creek at Huntsville (station 10137900), September 1985 through April 1987. .. 30 IIIII IIIII I I I I I t I I 0>

Approximate average discharge of Spring Creek, in cubic feet per second, determined from monthly measurements at site 4

Incremental discharge in Spring Creek drainage, in cubic feet per second, determined from monthly measurements at sites 1 to 3 and 5 to 7 25

0z 0 U 20 w (f) a: w a.. I- w W LL U 15 co ::::> U z u.i CJ a: « 10 I U (f) 0

5

o II =--t=-. I! + ~I I ~ II I 1--. 'i---"'" ~ III ~ NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN FEB MAR APR MAY JUNE 1984 1985 1986

Figure 8. Discharge determined from monthly measurements at seven sites in the Spring Creek drainage, November 1984 through June 1986. 2,000

1,000

o z South Fork Ogden River o near Huntsville, Utah () (station 10137500) w CIJ a: 100 w r I J I i Ii A 0- AJ! ,j :: ~ IP\ !I \ f­ ,: £ II :i r I 'i ~ W ill W \~ LL i \fh in !I'\ IViJ H ", L I I '. I' () ,;! CD \ ~ Ii ~ \ i\1~ I: :::::> \ , an! \ Ii!r i! , v,\ () ,=~i s~ i c: \ z I,. I'i'• I .. i• a \., 10 w C) " ! ~ 1I. \ 'I i \ II i\i: 1 a: ill d, ~ ~ i :\1 i'V \ « I:'I f\ ' ,• ;\ ,I• •• ,• ' I ,'"~,'A : .. I· : ~ () I l · I' W\.., .,,,!oJ"::li~·,J CIJ a.h.::i-i ! "."--, J...... , "'!:~: o ::i i : :./ Wheeler Creek / ( li i H z ~ ~ i "Be "oots."•. Utah , !; ! « IhI! (station 10139300) 11 I \. i w 'i ~ 1 I 1.1 j I ~ ~

0.1 JULY SEPT AUG OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT 1984 1985 1986

Figure 9. Daily mean discharge at the South Fork Ogden River near Huntsville (station 10137500) and at Wheeler Creek near Huntsville (station 10139300), July 1984 through September 1986 (discharge adjusted for diversions by city of Ogden). ... CD 44,000 acre-feet and covered about 1,800 acres when The Middle Fork Ogden River (stations fi lled. In 1957, the dam at Pineview Reservoir was 10137800 and 10137780; table 3) has relatively little raised 30 feet, and storage capacity in the reservoir flow during the irrigation season. The low flow is increased to 110,200 acre-feet. Pineview Reservoir diverted through a few ditches to the area northeast of covered about 2,900 acres when filled. The additional Pineview Reservoir. storage capacity was allocated for flood control, and the Weber Basin Conservancy District gained surface­ Water is diverted from the South Fork Ogden water rights to water in that storage (Blaine Johnson, River through canals and is used to irrigate much of the Ogden River Commissioner, oral commun., 1986). southern part of Ogden Valley. Water from the South Actual storage in the modified reservoir did not reach Fork Ogden River is diverted at three places. The larg­ the maximum until June 1962. Normal operating fluc­ est diversion, about 85 cubic feet per second, is about tuation of the reservoir pool for 1963-81 was about 25 0.5 mile downstream from the point where the South feet. The low stage usually occurs in late February or Fork Ogden River flows into Ogden Valley. About 80 early March, and the high stage usually occurs in June. cubic feet per second ofwater is diverted by canal to the north side of Ogden Valley, and about 5 cubic feet per Causey Reservoir is located in a narrow canyon second of water is diverted by pipeline to the south side east of Ogden Valley on the South Fork Ogden River of Ogden Valley (N.W. Plummer, Regional Director, above Beaver Creek. The reservoir provides water for U.S. Bureau of Reclamation, written commun., 1981). irrigation and for exchange rights for water wells in Ogden Valley (Blaine Johnson, Ogden River Commis­ The canals that divert water to the north side of sioner, oral commun., 1986). Filling of the reservoir Ogden Valley delivel' water to much of the area east and began in January 1966, and maximum storage capacity north of Huntsville. The largest canal from this diver­ sion, the Mountain Valley (or Ogden Valley) Canal, car­ was reached in April 1966. Causey Reservoir has a ries water along the northeast boundary of the valley storage capacity of6,870 acre-feet and covers 195 acres when filled. and delivers water to the Middle Fork Ogden River drainage and to the area east and south of Eden.

Irrigation and Other Diversions The pipeline that diverts water to the south side of Ogden Valley supplies the Roman Catholic Monas­ tery southeast of Huntsville with irrigation water for In 1925, about 11,150 acres were irrigated in alfalfa and small-grain fields. Water from Monastery Ogden Valley (Browning, 1925). A court decree in Spring [(A-6-2)27dcc-S II in upper Bennett Creek also 1948 indicated that about 10,550 acres were irrigated is used for irrigation of these fields. Excess water and (Judge John A. Hendricks, Second Judicial District of return water from the fields flows into the Huntsville the State of Utah, no. 7487,1948). In the mid-1960's, South Bench Canal (pI. 2), which supplies irrigation 12,050 irrigated acres were mapped (Haws and others, water to the area south of the South Fork Ogden River 1970, p. 109). In 1981, the irrigated acreage was about and Pineview Reservoir. 7,050 acres as determined for this study from aerial photography. This latest value probably represents a The other two diversions from the South Fork permanent decrease in irrigated acreage. Ogden River are minor. About I cubic foot per second of water is diverted from above the gaging station Water in the North Fork Ogden River is diverted (10137500; pI. 2) on the South Fork Ogden River, and at several places. The first major diversion from the about I cubic foot per second of water is diverted North Fork Ogden River flows into a storage pond that between the gaging station and the large diversion 0.5 feeds the Liberty Pipeline, which supplies water under mile downstream from where the South Fork Ogden pressure to sprinkler irrigation systems in much of the River flows into Ogden Valley. northern part of Ogden Valley. The West Ditch (pI. 2) diverts water from the Liberty Pipeline storage pond Water from WolfCreek is diverted at two places. and delivers water to irrigated land along the northwest­ Water from the upstream diversion is delivered to Wolf ern side of the valley. The Eden Canal (pI. 2) diverts Creek Resort north of Eden for irrigation of the golf water from the North Fork Ogden River, between Lib­ course and for culinary use. Water from the down­ erty and Eden, to irrigated land north of Pineview Res­ stream diversion is used to irrigate fields north and ervoIr. northwest of Eden.

20 Diversions from smaller watersheds and springs, possibly because Wheeler Creek flows through an area including Chicken Creek, Sheep Creek, Pole Canyon of the predominantly carbonate terrain. creek, Hawkins Creek, and Bennett Creek, also are used for irrigation. Ditches and canals that encircle the GROUND-WATER HYDROLOGY OF valley also capture some of the water that runs off the valley slopes. CONSOLIDATED ROCKS SURROUNDING OGDEN VALLEY Two pipelines divert water from Pineview Reser­ voir and Wheeler Creek. The first pipeline delivers The lithology and water-bearing characteristics water from Pineview Reservoir for hydroelectric­ ofthe consolidated rocks surrounding Ogden Valley are power generation and irrigation. The hydroelectric­ shown in table I. The consolidated rocks generally are power-generation plant has surface-water rights to all divided into five characteristic hydrogeologic units­ of the yearly natural flow in Ogden Valley, but the the Norwood Tuff, Wasatch Formation, carbonate delivery rate of water is limited to 260 cubic feet per rocks, clastic rocks, and metasedimentary rocks. second by the capacity of the pipeline. Between late April and early October, water in this pipeline also is The consolidated rocks surrounding Ogden Val­ distributed for irrigation outside of Ogden Valley ley that transmit and yield substantial quantities of (Blaine Johnson, Ogden River Commissioner, oral water are the Wasatch Formation and carbonate rocks. commun., 1986). The second pipeline delivers 15 to 20 The Wasatch Formation crops out over much ofthe area cubic feet per second of water (the working capacity of east ofOgden Valley (pI. I) and is at depth south ofand the Ogden City Water Utilities filtration plant) from beneath parts of Ogden Valley. The carbonate rocks Pineview Reservoir and Wheeler Creek to Ogden crop out over a large area in the upper South Fork between May and October (Gary Clark, Ogden City Ogden River drainage above Causey Reservoir and in Water Utilities, oral commun., 1986). smaller areas west of Liberty; south and northeast of James Peak; and west, southwest, and southeast of Water Quality Pineview Reservoir (pI. I). The dissolved-solids con­ centration of water in the consolidated rocks is less than Surface-water samples were collected at 10 loca­ 250 milligrams per liter and the water is a calcium tions throughout Ogden Valley and the surrounding bicarbonate type. area by Thompson (1983). Streams were sampled early and late in the irrigation season. The dissolved-solids Recharge concentration for all samples, except those from Spring Creek, was less than 200 milligrams per liter during the Much of the recharge to consolidated rocks in the springtime high flows. Spring Creek derives much of its flow from ground-water discharge. In August, the uplands surrounding Ogden Valley probably originates dissolved-solids concentrations more than doubled from snowmelt that infiltrates the Wasatch Formation. because of irrigation losses as the water was reused. All The 1931-60 average annual precipitation in the South water was a calcium bicarbonate type. Fork Ogden River drainage is about 7.54 billion cubic feet; the average annual precipitation in the Wheeler Specific conductance and water temperature for Creek drainage is about 784 million cubic feet. many of the streams in Ogden Valley and the surround­ ing area were measured during base-flow periods Few data are available on recharge from losing (tables 4 and 5). The specific conductance of all sam­ streams or subsurface inflow from adjacent areas. A ples was less than 400 microsiemens per centimeter, seepage run made October 17, 1985, indicated that which relates to a dissolved-sol ids concentration of less Wheeler Creek was losing about 0.4 cubic feet per sec­ than about 250 milligrams per liter. Data from the ond between the lower part of Snow Basin and the lower North Fork Ogden River Basin (sites N II and Ogden River. Relatively little recharge to the consoli­ N 13) and from Liberty Spring Creek (table 4) show dated rocks occurs by subsurface inflow from adjacent warmer water temperatures that may result from ground-water systems because much of the area sur­ ground-water seepage. Water in Wheeler Creek (table rounding Ogden Valley is topographically higher than 5) has relatively large specific-conductance values, the adjacent areas.

21 Table 4. Miscellaneous measurements of streamflow, specific conductance, and water temperature during base flow in Ogden Valley, February 23 to March 1, 1985

[N I, miscellaneous measurement site on North Fork Ogden River; M I, miscellaneous measurement site on Middle Fork Ogden River; S I, miscellaneous measurement site on South Fork Ogden River; -, no data]

Specific Site Drainage basin and location Streamflow conductance Water number of measurement site (cubic feet (microsiemens temperature (pI. 2) per second) per centimeter (degrees at 25 degrees Celsius) Celsius)

North Fork Ogden River drainage

NI North Fork Ogden River, 200 feet above diversion gate, sec. I, T. 7 N., R. IW 10.4 115 1.5 N2 Cobble Creek, below road culvert, sec. 7, T. 7 N., R. 1 E .4 91 2.0 N3 North Fork Ogden River, 200 feet above County Highway 162 bridge, sec. 7, T. 7 N., R. IE 8.0 115 a N4 Spring flow, measured alongside County Highway 162 under powerlines, sec. 20, T. 7 N., R. IE 1.4 330 5.0 N5 Diversion ditch from Liberty Spring Creek (north of main channel), east of road culvert, sec. 19, T. 7 N., R. IE 1.4 315 9.0 N6 Liberty Spring Creek (main channel), upstream of road culvert, sec. 19, T. 7 N., R. IE 3.5 290 8.5 N7 Liberty Spring Creek (south channel, flow in winter primarily from bedrock springs to the south), 400 feet downstream from road culvert, sec. 19, T. 7 N., R. IE .6 350 3.5 N8 Pine Creek, above County Highway 162 culvert, sec. 28, T. 7 N., R. IE .2 265 2.0 N9 Pole Canyon creek, below County Highway 162 culvert, sec. 28, T. 7 N., R. IE .5 205 .5 NIO Liberty Spring Creek, above confluence with North Fork Ogden River, sec. 28, T. 7 N., R. IE 13.0 325 8.0 Nil North Fork Ogden River above confluence with Liberty Spring Creek, sec. 28, T. 7 N., R. IE 73 145 7.5 NI2 Wolf Creek, below County Highway 162 culvert, sec. 28, T. 7 N., R. IE 3.6 275 3.0 NI3 North Fork Ogden River, 100 feet above County Highway 162 bridge, sec. 34, T. 7 N., R. 1 E 18.0 260 6.0 Middle Fork Ogden River drainage MI Middle Fork Ogden River, 200 feet above road bridge, sec. 5, T. 6 N., R. 2 E 8.5 155 0 M2 Middle Fork Ogden River, at discontinued gaging station 10137800, below County Highway 166 bridge, sec.I,T.6N.,R.I E 4.2 170 2.0

22 Table 4. Miscellaneous measurements of streamflow, specific conductance, and water temperature during base flow in Ogden Valley, February 23 to March 1, 1985-Continued

Specific Site Drainage basin and location Streamflow conductance Water number of measurement site (cubic feet (microsiemens temperature (pI. 2) per second) per centimeter (degrees at 25 degrees Celsius) Celsius)

Middle Fork Ogden River drainage-Continued

M3 Small channel north of main Middle Fork Ogden River channel, below County Highway 166 culvert, sec. I, T. 6 N., R. IE 0.2 M4 Geertsen Canyon creek, above County Highway 166 bridge, sec. 36, T. 7 N., R. IE 2.8 100 3.0 M5 Small channel west of Geertsen Canyon creek, above County Highway 166 culvert, sec. 36,T. 7 N., R. IE 2.9 245 0 M6 Second small channel west of Geertsen Canyon creek, in County Highway 166 culvert, sec. 2, T. 6 N., R. IE .1 M7 South branch Dry Hollow Creek, above County Highway 166 bridge, sec. 6, T. 6 N., R. 2 E .3 M8 North branch Dry Hollow Creek, 300 feet below County Highway 166 bridge, sec. I, T. 6 N., R. IE .7 230 2.5 M9 Small channel south of Dry Hollow Creek, above County Highway 166 bridge, sec. 7, T. 6 N., R. 2 E .4 MID Kelley Canyon creek, 30 feet above road culvert, sec. 9, T. 6 N., R. 2 E .2 335 1.5 MIl Maple Canyon creek, above road culvert, sec. 9, T. 6 N., R. 2 E .5 130 1.5 South Fork Ogden River drainage

SI Spring flow in channel, above County Highway 39 culvert, sec. II, T. 6 N., R. 2 E .9 64 3.5 S2 Quarry Hollow creek, above road culvert south of Monastery, sec. 22, T. 6 N., R. 2 E 1.4 265 .5 S3 Bennett Creek, 300 feet below bridge, sec. 21, T. 6 N., R. 2 E 2.4 270 D S4 Huntsville South Bench Canal (Bennett Creek), above diversion structure at Bally Watts Creek confluence, sec. 21, T. 6 N., R. 2 E 8.9 375 3.5

23 Table 5. Miscellaneous measurements of streamflow, specific conductance, and water temperature during base flow, upper Middle Fork Ogden River, October 1984, and Wheeler Creek, October 1985

[--, no dutu]

Specific Drainage basin and location Streamflow conductance Water of measurement site (cubic feet (microsiemens temperature per second) per centimeter (degrees at 25 degrees Celsius) Celsius)

Upper Middle Fork Ogden River drainage

Right Fork, Middle Fork Ogden River, upstream of confluence with springflow, sec. 30, T. 8 N., R. 3 E 1.4 365 6.0

Springflow (originating in sec. 25, T. 8 N., R. 2 E.), sec. 30, T. 8 N., R. 3 E .1 365 7.0

Right Fork, Middle Fork Ogden River, upstream of confluence with springflow, sec. 6, T. 7 N., R. 3 E 1.7 345 8.5

Springflow (originating in sec. 31, T. 8 N., R. 3 E.), sec. 6, T. 7 N., R. 3 E .4 340 7.5

Right Fork above confluence with Left Fork, Middle Fork Ogden River, sec. 14, T. 7 N., R. 2 E 2.1 285 10.0

Left Fork above confluence with Right Fork, Middle Fork Ogden River, sec. 14, T. 7 N., R. 2 E .5 130 9.5

Springflow (originating in sec. 4, T. 7 N. R. 2 E.), sec. 14, T. 7 N., R. 2 E .4 134 10.0

Middle Fork Ogden River at trail crossing, sec. 27, T. 7 N., R. 2 E 3.5 240 11.0

Middle Fork Ogden River above first diversion structure, sec. 33, T. 7 N., R. 2 E 4.2 255 12.0

Wheeler Creek drainage

Wheeler Creek, below marshy area, sec. 29, T. 6 N., R. IE 1.0 375 4.0

Middle Fork Wheeler Creek, at road crossing, sec. 28, T. 6 N., R. IE .1

Wheeler Creek above East Fork Wheeler Creek confluence, sec. 22, T. 6 N., R. IE 1.0 395 4.0

East Fork Wheeler Creek above road crossing, sec. 27, T. 6 N., R. IE .2 810 4.5

East Fork Wheeler Creek above Wheeler Creek, sec. 22, T. 6 N., R. IE .1

Wheeler Creek at gaging station 10139300, sec. 16, T. 6 N., R. IE .9 440 9.0

24 Discharge Average monthly flow and daily minimum flow for upper Middle Fork Ogden River drainage (upstream from station 10137780) Discharge from the consolidated rocks is by streams, evapotranspiration, springs, subsurface out­ flow, and wells. Discharge from the consolidated rocks Average Average to streams was estimated by analysis of streamflow monthly daily records of low-flow conditions in the late fall and win­ Month flow minimum flow ter. Presumably, most of the flows recorded during (cubic feet (cubic feet low-flow conditions represent ground-waterdischarge. per second) per second) In addition, a seepage run was made on the Middle Fork Ogden River. November 4.1 2.8 5.8 3.8 The average monthly flow in the upper North December Fork Ogden River drainage, upstream from station January 8.5 4.9 10137680, determined for the base-flow period February 9.9 7.4 November through February for water years 1964-74, was about 5 cubic feet per second. Ground-water dis­ charge to the stream, as indicated by the average daily minimum flow, increased from 3.2 to 4.1 cubic feet per The average monthly flow in the South Fork second from November to February. Ogden River drainage, upstream from station 10137500 (generally the South Fork Ogden River Average monthly flow and daily minimum flow for upper North Fork Ogden River drainage (upstream from station watershed upstream from Ogden Valley), determined 10137680) for the base-flow period November through February for water years 1922-65 (before Causey Reservoir dam was constructed), was about 43 cubic feet per second. Average Average monthly daily Discharge of Causey Spring accounts for about 21 Month flow minimum flow cubic feet per second or nearly 50 percent of the base (cubic feet (cubic feet flow in the South Fork Ogden Riverdrainage. The base per second) per second) flow in Beaver Creek, which enters the South Fork Ogden River downstream from Causey Reservoir, has Novcmher 4.6 3.2 never been recorded but probably is about 2 cubic feet Deccmhcr 4.4 3.3 per second. Therefore, the maximum possible dis­ January 55 3.5 charge ofground water to the South Fork Ogden River, Fchmary 5.0 4.1 upstream from station 10137500, is about 20 cubic feet per second.

The average monthly gain in flow to the South The average monthly flow in the upper Middle Fork Ogden River between Causey Reservoir dam and Fork Ogden River drainage, upstream from station station 10137500 was determined from the flow records 10137780, determined for the base-flow period November through February for water years 1964-74, collected at stations 10137300 and 10137500 from increased from 4.1 to 9.9 cubic feet per second. November through February for water year 1967. Bea­ Ground-water discharge to the stream, as indicated by ver Creek, which is the only substantial source of sur­ the average daily minimum flow, increased from 2.8 to face-water inflow to the South Fork Ogden River in this 7.4 cubic feet per second. reach, is assumed to consist of only base flow from November through February. The gain in flow to the A seepage run made October II, 1984, on the South Fork Ogden River and the base flow of Beaver upper Middle Fork Ogden River indicated a gain of Creek are the estimated ground-water inflow to the about 1.4 cubic feet per second between the upstream South Fork Ogden River drainage upstream from reaches of the river and Ogden Valley. Ogden Valley for water year 1967. The estimated inflow by month is as follows:

25 1)32acc-S1], Monastery Spring and its associated Estimated ground-water springs [(A-6-2)27dcc-Sl], Patio Springs [(A-7- inflow Month (cubic feet 1)22caa-S 1], Burnett Spring [(A-7-1 )22dad-S1], Cau­ per second) sey Spring [(A-7-3)23acb-Sl], and Limestone Spring [(A-8-3)34caa-S 1] (table 6). Carbonate rocks are the November 7.6 source for Wheeler Spring and Causey Spring. Monas­ December 9.5 January 10.8 tery Spring, its associated springs, and Limestone February 14.6 Spring appear to have their sources in the Wasatch For­ mation or possibly the carbonate rocks. Patio Springs probably issues from the Wasatch Formation. The The average monthly discharge from the Wheeler Creek drainage at station 10139300 (pI. I), determined water of Burnett Spring is from the Norwood Tuff but for the base-flow period November through February ultimately may be derived from the metasedimentary for water years 1958-84, increased from about 2.1 cubic rocks. Liberty Spring [(A-7-1)19dbc-SIl discharges feet per second in November to 5.0 cubic feet per sec­ from the valley-fill deposits, but the source of the water ond in February. The average daily minimum flow, probably is subsurface inflow from nearby carbonate which is the best estimate of ground-water discharge to rocks (fig. 10). the stream, fluctuated slightly through the period of analysis. Innumerable small springs discharge throughout Average monthly flow and daily minimum flow for Wheeler the area. All ofthe community water-supply systems in Creek (station 10139300) the upper drainage area and a number of the municipal water-supply systems in Ogden Valley derive their Average Average water from the small springs in consolidated rock. monthly daily Springs issuing from the Wasatch Formation irrigate flow minimum flow Month about 50 acres in the Sheep Herd Creek valley south­ (cubic feet (cubic feet per second) per second) east of Huntsville.

November 2.1 1.3 Some wells in Ogden Valley also derive water December 2.1 1.2 from the consolidated rocks. Wells completed in the January 2.7 1.1 Wasatch Formation include a flowing well at the Wolf February 5.0 1.4 Creek Resort north of Eden, a community well west of the resort well, a rarely-used community well south­ west of Huntsville, and other individual small-yield Evapotranspiration and subsurface outflow from wells in the upper South Fork Ogden River drainage. the bedrock can be estimated by comparing precipita­ tion and streamflow records. The 1931-60 average Ground water in the Wasatch Formation commonly is annual precipitation in the South Fork Ogden River under confined conditions, and several wells flow. One drainage area above station 10137500 was 7.54 billion community well and a few domestic wells along the cubic feet. The average annual discharge of the South margin and foothills of Ogden Valley yield small quan­ Fork Ogden River at station 10137500 during 1931-60 tities of water from the Norwood Tuff. Relatively few was 3.33 billion cubic feet. Thus, an annual average of wells in the area surrounding Ogden Valley pump water 4.21 billion cubic feet (133 cubic feet per second) from the bedrock. evapotranspired or recharged the valley-fill aquifer sys­ tem by underflow in the alluvium of the South Fork A few wells derive water from the other hydro­ Ogden River channel. This is an average areal rate of geologic units (table 7). Well (B-8-1 )36dcc-l, which is about 13.2 inches per year. The same analysis on the in the uppermost part of the North Fork Ogden River Wheeler Creek drainage for precipitation from 1931-60 drainage and yields about 20 gallons per minute, prob­ and streamflow from 1958-86 yields an average areal ably is completed in the Mutual Formation of Precam­ rate of about 18.9 inches per year. brian age. A few wells south of the South Fork Ogden The major springs that issue from the consoli­ River canyon mouth may be completed in carbonate dated rocks in the study area are Wheeler Spring [(A-6- rocks.

26 Figure 10. Liberty Springs (arrow) at Liberty, Utah (looking east from hillside on Wasatch Range toward Bear River Range).

GROUND-WATER HYDROLOGY The term "principal aquifer" is used in this report OF VALLEY-FILL DEPOSITS IN to refer to the confined aquifer in the center of the OGDEN VALLEY southern part of the valley as well as the unconfined parts ofthe aquifer in the northern part ofOgden Valley The areal extent of the unconsolidated valley-fill and along the margins ofthe southern part ofthe valley. deposits in Ogden Valley is about 40 square miles. The term "shallow water-table aquifer" refers to the These deposits are saturated and constitute a major upper unconfined aquifer that overlies the confined part aquifer system which is referred to as the valley-fill ofthe principal aquifer in the center ofthe southern part aquifer system in this report. Slopewash and other rel­ of the valley. The term "valley-fill aquifer system" atively thin saturated deposits on the mountain slopes refers to the entire ground-water reservoir in the valley­ also are part of the valley-fill aquifer system. fill deposits (table 1) of Ogden Valley.

Ground-water conditions vary throughout the valley. In the northern part of Ogden Valley and along Recharge the margins of the southern part of the valley, the ground water is unconfined although, locally, perched Precipitation, seepage from streams and canals, ground water may occur above the water table. Near excess irrigation water, and subsurface inflow recharge the center of the southern part of the valley, two rela­ the valley-fill aquifer system. Direct infiltration from tively distinct aquifers are separated by an intervening snowmelt and seepage from stream channels are the silty clay layer. Ground water in the lower aquifer is major sources of recharge during the spring freshet. confined and is pumped intensively in Ogden Valley. During the remainder of the year, subsurface inflow Ground water in the upper aquifer is unconfined and from bedrock and infiltration of irrigation water proba­ few wells withdraw water from it. bly are the major sources of recharge.

27 Table 6. Records of springs

[-, no data]

Location: See figure 2 for description of data-site numbering system. Aquifer: See table I for explanation of code and description of lithology. Use of water: H, domestic; I, irrigation; P, public supply; R, recreation; U, unused. Discharge: E, estimated.

Use Altitude Specific of of land conductance Location User Aquifer water surface Discharge (microsiemens (feet) (gallons per centimeter per minute) at 25 degrees Celsius)

(A-6-1)15dbd-SI Forest Service 123NRWD P 5,370 (A-6-1 )25aab-S I Huntsville Water Co. 123NRWD P 5,120 (A-6-1 )32acc-S I Snow Basin 300cRSL P 6,480 240 250 (A-6-2)IOccd-S I 400PCMB H 5,160 3.3 425 (A-6-2)llddc-S I Fraternal Order of Eagles 400PCMB P 5,160 45 E (A-6-2)12dac-SI Forest Service 400PCMB P 5,220 4 295 (A-6-2)17bdb-S 1 IIIALVM U 4,940 975 450 (A-6-2)27cda-S I Huntsville Water Co. I24WSTC P 5,240 17 420 (A-6-2)27dcc-S I Roman Catholic Church and 300cRSL I,P 5,320 710 430 Huntsville Water Co. (A-6-2)27dcc-S2 Huntsville Water Co. 300cRSL P 5,280 27 435 (A-6-3) 5acb-SI Forest Service IIIALVM U 5,390 13 345 (A-6-3) 5bdc-SI Forest Service IllALVM P 5,400 (A-6-3)23acb-S 1 Causey Estates I24WSTC P 7,760 (A-6-3)23ada-S I Causey Estates I24WSTC P 7,680 (A-6-3)23adb-S I Causey Estates I24WSTC P 7,680 (A-6-3)23daa-S I Causey Estates I24WSTC P 8,080 (A-7-1) labb-SI Powder Mountain Water Dist. IllALVM P 8,120 6 53 (A-7-1) labd-SI Powder Mountain Water Dist 300cRSL P 7,920 9 415 (A-7-1) Iddb-SI Powder Mountain Water Dis!. 300cRSL P 7,600 110 405 (A-7-1) 12acb-S I 300cRSL U 7,200 100 275 (A-7-1) 19dbc-S 1 Shupe, Thomas lllALVM I 5,170 900 E 280 (A-7-1)22caa-SI WolfCreek Resort I24WSTC I,R 5,260 175 (A-7-1)22dad-SI Eden Water Assoc. 123NRWD P 5,320 (A-7-1)30aca-SI Spring Mountain Ranch 371SCRL P 5,430 195 340 (A-7-I )30baa-S I Shupe, Thomas 371SCRL P,I 5,400 700 E 360 (A-7-3)4abb-SI Sourdough Ranch I24WSTC P 7,660 3.7 390 (A-7-3) 4baa-SI Sourdough Ranch I24WSTC P 7,640 4.7 355 (A-7-3)23acb-SI 33IHMBG U 6,440 9,800 285 9,800 365 (A-7-3)26acb-S I Boy Scouts of America 337LDGP U 5,750 695 460 (A-7-3)28bba-SI Nass, Tom I24WSTC I 5,720 73 360 (A-7-3)34cbc-SI Weber County I24WSTC U 5,520 150 400 (A-8-2)35dac-S I Sunridge, Inc I24WSTC P 7,800 70 375 (A-8-3)22cdc-S I I24WSTC U 7,030 6 360 (A-8-3)3Ibd -SI Sunridge, Inc I24WSTC P 7,340 5 (A-8-3)34caa-S I I24WSTC U 6,660 250 E 415 (B-7-1)2caa-SI Cobblecreek Park 400PCMB P 5,940 33 240 (B-8-1 )34daa-S I Liberty Pipeline Co. 400PCMB P 6,080 (B-8-1 )34daa-S2 Liberty Pipeline Co. 400PCMB P 6,120 (B-8-1 )34dab-S I Liberty Pipeline Co. 400PCMB P 6,140 (B-8-1 )34dba-S I Liberty Pipeline Co. 400PCMB P 6,200 (B-8-1 )36cba-S I American Baptist Church 400MUTL P 5,660 5

28 29 Table 7. Records of wells

[-, no data]

Location: See figure 2 for explanation of data-site numbering system. Owner: Owner at time well was visited by U.S. Geological Survey personnel or as listed by driller on Utah well-completion report. Finish: P, perforated casing below depth to first opening; S, screened casing below depth to first opening; X, open hole below Use of water: C, commercial; H, domestic; I, irrigation (predominately lawn and garden watering); P, public supply; S, stock; U, Type of lift: C. centrifugal; F, natural flow; J, jet; S, submersible; T, turbine. Type of power: D, diesel; E, electricity. Aquifer: See table I for explanation of code and description of lithology. Water level: Below or above (-) land surface; F, reported as flowing, no water level. Specific capacity: Discharge in gallons per minute per foot of drawdown. Number in parentheses is duration of test in hours. All Other data collected during study by U.S. Geological Survey personnel: WL (water levels)-C, continuous; M, monthly; 0, one QW (water quality)-A, specific conductance and temperature in table 8; 0, chemical analysis done in 1985 shown in table 8; B,

Depth to Use Type Type Date Depth first of of of Location Owner drilled of well opening Finish water lift power (feet) (feet)

(A-6-1) 1aaa-I Hinkley Ranch 1932 19.5 U (A-6-1)lbaa-1 Graham, Olga 08/25/1977 126 100 P H,I S E (A-6-1) Idad-I Argyle, Dell 12/12/1975 100 95 P H,S,I S E (A-6-1 )3dbc-1 Adams, Glen 06/05/1967 187 140 P H,I S E (A-6-1)lOaac-1 Ogden Pineview Yacht Club 155 P,I SE (A-6-1)IOdbc-1 Radford, Edward 08/14/1969 142 124 P P,I SE (A-6-1) IOdbd-1 Radford, Edward 09/1211969 130 114 PP (A-6-1)IOdda-1 Forest Service 10/31/1963 169 149 P U SE (A-6-1)llacb-1 Evergreen Ranch 04/30/1968 151 U (A-6-1)llbdd-1 Ogden City 10/01/1971 400 P P T E (A-6-1)llbdd-2 Ogden City 400 P T D (A-6-1) Ilcab-I V.S. Geological Survey 10/11/1952 210 146 P V

(A-6-1) Ilcab-I V.S. Geological Survey 10/11/1952 323 222 P V (A-6-1)llcab-2 Ogden City 229 176 SP T E (A-6-1) Ilcab-3 Ogden City 511 206 P P T E (A-6-1) Ilcab-4 Ogden City 03/16/1971 400 PP T E (A-6-l)llcba-1 Ogden City 02/14/1969 237 202 S V (A-6-1)llcba-2 Ogden City 1970 239 201 SP T D (A-6-1)lldbd-1 Ogden City 1932 90 90 X V (A-6-1)lldbd-2 Ogden City 09/00/1932 68 68 X V (A-6-1)1ldbd-3 Ogden City 09/00/1932 4 4 X V (A-6-1)lldcd-1 V.S. Geological Survey 10/10/1935 152 152 X V (A-6- t)ll dcd-2 Forest Scrvice 1 t/01/1955 190 170 PP S E (A-6-1) 12aad-1 Ogden City 1932 108 108 X V (A-6-1)12dcd-1 Ceibert, Peter OS/20/1960 145 138 P U (A-6-1) 13cdd-1 Forest Service 06/28/1961 133 110 PP S E (A-6-1) 14ccd-1 Adams, A. Paul 09/24/1981 335 85 P V (A-6-1) 15dbc-1 Forest Service 450 P (A-6-1 )22dab-1 Webber, John 06/00/1976 122 60 PH S E (A-6-1 )23adb-1 Lakeview Water Co. 04/01/1960 500 P S E (A-6-1 )23dbc-1 Webber. John 1976 250 210 P H S E (A-6-1 )24aba-2 Lakeview Water Co. 07/06/1969 197 130 P P S E (A-6-2)5bac-1 Jensen Ranch S.Z,H S E (A-6-2l5bbc-1 Jensen. Rick 54 H.I SE (A-6-2)5bcc-1 Jensen Ranch 10/01/1952 50 30 P S.Z SE (A-6-2)6aab-1 Hinkley Ranch 120 U (A-6-2)6bbb-1 Hinkley Ranch 10/19/1964 227 60 P S.H.I T E (A-6-2)6cad-1 Erekson. Affd 05/01/1981 103 100 P U (A-6-2)6dad-1 Kotter. David 12/00/1977 100 100 X H.I SE

30 depth to first opening. unused; Z, dairy sanitation.

data obtained from Utah well-completion reports unless otherwise specified. time or random; S, semiannual. chemical analysis prior to 1985 shown in table 8.

Date Specific Altitude water Discharge Date capacity Other data of land Water level (gallons discharge (gallons per available Aquifer surface level measured per measured minute per foot WL QW Remarks (feet) (feet) minute) of drawdown)

IIIALVM 4,920 S 112ALVM 4,921 30 10/03/1977 7 .1(2) M 112ALVM 4,933 35 25 .3(2) S a 112ALVM 4,960 28 06120/1967 10 06100/1967 S 112ALVM 4,925 S 112ALVM 4,980 38 09/10/1969 15 15 (12) S These two wells supply water to 112ALVM 4,940 30 09/19/1969 20 20 (12) houses on Forest Service land. 112ALVM 4,907 32 11/29/1963 M Port Ramp well. 112ALVM 4,915 47 05/10/1968 10 .6(2) M 112ALVM 4,900 43 12/15/1971 2,500 50 (24) Well 5. 112ALVM 4,900 43 2,500 50 (24) Well 6. 112ALVM 4,915 M Two wells at same site. Water-level data for both 112ALVM 4,915 250 12111/1952 125 M wells back to 1953. 112ALVM 4,895 Well 2. 112ALVM 4,910 a Well 3. 112ALVM 4,895 43 2,500 50 Well 4. 112ALVM 4,905 30 04129/1969 2,500 26 (6) Test well, now plugged. 112ALVM 4,910 Weill. 112ALVM 4,832 -10.06 09/15/1932 B Well 102, now plugged. 112ALVM 4,833 -9.66 09/3111932 B Well 101, now plugged. IIIALVM 4,832 .14 09125/1932 B Well 100, now plugged. 112ALVM 4,881 Cemetery well, now plugged. 112ALVM 4.915 180 60 (1.5) MB Bluff well. 112ALVM 4,880 7.58 0912011932 B Tower well, now plugged. 112ALVM 4.920 42 1012111960 8 2.6(4) S 112ALVM 4,921 26 07/0111961 60 M Anderson Cove well. 123NRWD 5,240 60.3 07/3111984 1.5 <.1(2) a 123NRWD 5,439 90 08/01/1985 a 123NRWD 5,950 41.3 08118/1984 100 a 123NRWD 5,120 4 175 1.7 B Secondary well. 123NRWD 5,550 1556 08/1811984 45 a 112ALVM 4,930 29 07117/1969 164 2.4(7) S Primary well. 5,110 Provides water 10 dairy farm. IIIALVM 5,020 S IIIALVM 5,000 14 25 10/1611952 4.2 IIIALVM 5,010 M 112ALVM 4,945 8 02/15/1965 100 05120/1965 .7(2.5) S 112ALVM 4,945 18 06/30/1981 15 06/00/1981 3.0(1) S IIIALVM 4,970 30 12/0011977 15 S a

31 Table 7. Records of wells-Continued

Depth to Use Type Type Date Depth first of of of Location Owner drilled of well opening Finish water lift power (feet) (feet)

(A-6-2)6dda-1 Montgomery, Norman 01/09/1964 51 36 P S,H,Z S E (A-6-2)7aab-1 Skeen, Joseph 07/16/1968 92 92 X H,I S E (A-6-2)7bbb-1 Newey, Dale 12/23/1957 III 85 P S,Z,H S E (A-6-2)7bbd-1 Casey Acres Subdivision 08/02/1980 110 90 P V (A-6-2)7bbd-2 Casey Acres Subdivision 09/21/1980 130 105 P P E (A-6-2)7bcc- I Quist, Ivan 10/03/1965 102 100 X H,I SE (A-6-2)7cad-1 Clawson, Jack 01/00/1978 120 105 P H,I SE (A-6-2)7dac-1 Ekstrom, Don 8 X V (A-6-2)7ddb-1 McKay, John 05/00/1968 107 H,S,I SE (A-6-2)8ddb-1 Shafer OS/22/1970 160 100 P I,H CE (A-6-2)9cac-1 Green Hill Estates 04/01/1979 240 120 PP SE (A-6-2) 14bab-1 Fraternal Order of Eagles 04/00/1972 257 105 P V (A-6-2) 14bbd-1 Cox, David 07/31/1984 100 88 P H SE (A-6-2)14bcc-1 Hunter, David 06/15/1979 112 100 P H,S,I SE (A-6-2) 15acb-1 Vtah Dept. of Transportation 1973 285 158 P H,I SE (A-6-2) 15cdb-1 Odekirk, Forrest 06/05/1978 98 82 P H,I SE (A-6-2)16ada-1 Weems, S.L. 11/02/1954 242 84 I,H,S TE (A-6-2)16add-1 Field, Joe 03/23/1979 220 172 P H,I SE (A-6-2) 16bad-1 Verhaal, Richard 03/22/1979 101 80 P H,I SE (A-6-2)16bdb-1 Carrick, David 08/24/1984 115 105 PH SE (A-6-2) 16cbd-1 Walker, Hugh 10/20/1976 100 90 P H,I SE (A-6-2)16dad-1 Gay, Larry 10/06/1960 54 54 X H,I,S SE (A-6-2) 17aab-1 Toyn, Robert 11/05/1958 42 37 P H,I,C SE (A-6-2) 17abb-1 Wood, Robert 06/13/1977 100 90 P H,I SE (A-6-2) 17bbb-1 Argyle, Dell 08/08/1956 40 35 P H,S F (A-6-2)l7cca-1 Schade, Marlon 04/25/1970 124 86 P H,I SE (A-6-2)17dac-1 Allen, Lila 05/00/1974 102 H,I SE (A-6-2)17dbd-1 Allen, Garth 40 H,I,S SE (A-6-2) 18bad-1 V.S. Bureau of Reclamation 11/08/1955 155 105 P V (A-6-2)18dad-1 American Legion 11/08/1967 87 87 X C,I,H SE (A-6-2) 18dad-2 Andrews, Raymond 07/01/ I981 103 82 P H,I S E (A-6-2) 18dbb-1 Deatherage, D. 18 18 X U (A-6-2) 19abb-1 Forest Service 06/30/1961 69 26 PP SE (A-6-2) 19bda-1 Wangsgard, William 120 C,H,I SE (A-6-2)I9bdb-1 Peterson, Chris 08/07/1961 90 C,P,I SE (A-6-2)20acd-1 Wangsgard, Clark 06/23/1978 86 66 P V (A-6-2)20bad-1 Froerer Dairy Farm 04/25/1969 86 86 X S,Z,H SE (A-6-2)2Iaab-1 Lowe, John H,I,S SE (A-6-2)21 abc-I Birch, Ralph 09/23/1942 37 V (A-6-2)21 abc-2 Osmond, Dennis 12/26/1979 101 91 P U (A-6-2)2Iacd-1 Kenley, Wayne 07/30/1971 79 79 X H,S SE (A-6-2)21 bbb-I Wangsgard Ranch 12/05/1956 81 72 P S,Z,H SE (A-6-2)2Icbd-1 Messerly, Grant 04/21/1970 105 38 P H,I,S SE (A-6-2)2Iccd-1 Mertz, Brian 06/08/1984 170 155 P H,S,I S E (A-6-2)22bcb-1 Roman Catholic Church 36 H JE (A-6-2)28aaa-1 Russell, Scott 08/00/1976 220 120 P H S E (A-6-2)28aba-1 Stoddard, Dougla~ 07/18/1973 140 P H,I SE (A-6-3)5abb-1 Read, Boyd 11/18/1953 74 66 PP S E (A-7-1)6dda-1 Shaum, Robert 07/10/1972 142 40 P H,S SE (A-7-1)7abc-1 Elliot, Charles 07/12/1973 160 143 X H,I SE (A-7-1)7dba-1 Quist, Farley 08/04/1975 102 80 P H,I SE (A-7-1)7dcb-1 Zwahlen, Carl 07/17/1973 224 H,I SE (A-7-1)7dda-1 Van Alfen, John 12/00/1978 140 100 P H,I S E (A-7-I )8cad-1 Roberts, Emil 01/01/1976 180 S SE (A-7-1)8cbb-1 Nelson, Ralph 06/27/1967 120 57 P I,H,S SE

32 Date Specific Altitude water Discharge Date capacity Other data of land Water level (gallons discharge (gallons per available Aquifer surface level measured per measured minute per foot WL OW Remarks (feet) (feet) minute) of drawdown)

IIIALYM 4,970 24 02/03/1964 60 20 (2.5) Provides water to dairy farm. IllALYM 4,950 26 07/3011968 8 .6(2) S IIIALYM 4,924 45 20 12/3011957 1.3 S Provides water to diary farm. IIIALYM 4,926 20 08/02/1980 500 S 112ALYM 4,930 23 10/09/1980 60 1010911980 30 (1) 112ALYM 4,922 18 10/2611965 6 S 0 112ALYM 4,940 32 01/00/1978 20 01/0011978 S IIIALYM 4,930 S 112ALYM 4,920 F 08/02/1968 S 0 112ALYM 4,970 15 0511211970 30 2.0(1) M 0 123NRWD 5,030 25.3 07/3111984 90 0 112ALYM 5,120 7 1010011973 5 10100/1973 <.1(3) S IIIALYM 5,090 38 08/22/1984 15 08/0011984 .5(1) S 0 IIIALYM 5,085 35 06/29/1979 30 2.0(1) S 112ALYM 5,060 43 08/22/1973 50 .6(24) M 0 IIIALYM 5,040 16 0611611978 10 2.0(2) S 0 112ALYM 5,025 39 150 12117/1954 1.2 112ALYM 5,025 45 08/25/1979 18 .6(1) S IIIALYM 4,990 26 0412511979 10 2.0(2) S 0 112ALYM 4,980 20 0912611984 15 1.5(2) S IIIALYM 4,985 22 11115/1976 10 1.0(2) S IIIALYM 5,025 37 10/1811960 5 10/18/1960 .8(2) S IIIALYM 4,970 II S 112ALYM 4,955 16 30 S IIIALYM 4,930 -5 08/0911956 20 08/0911956 S A 112ALYM 4,940 37 25 05/06/1970 .7(1) S 0 112ALYM 4,970 2 06/00/1974 150 06/0011974 S 0 IIIALYM 4,970 S 112ALYM 4,918 35 60 11128/1955 .8 CB Well on County Highway property. 112ALYM 4,940 20 12/02/1967 10 .4(2) 112ALYM 4,935 20 09/1811981 10 .7(2) M IIIALYM 4,925 S 112ALYM 4,900 07/0411961 60 6.0(1) SA IIIALYM 4,960 S Trappers Inn Restaurant. IIIALYM 4,960 50 09/0111961 5 .6(1) Chris's Gas Station and Bar. 112ALYM 4,950 F 07/14/1978 30 07/14/1978 SA 112ALYM 4,955 4 05/02/1969 10 3.3(2) Provides water to dairy farm. 5,01D S IIIALYM 5,000 24 09/0011942 M 112ALYM 5,000 16 01128/1979 75 1.9(2) M 112ALYM 4,990 13 08/06/1971 10 .5(2) S 0 112ALYM 4,980 15 25 12/10/1956 2.5 S Provides water to dairy farm. 112ALYM 4,990 12 05128/1970 10 .3(2) S IIIALYM 5,040 38 10/04/1984 4 <.1(2) S IIIALYM 5,005 S 124WSTC 5,020 F 08/3111976 II 08/3111976 M 112ALYM 5,030 2 S 0 124WSTC 5,330 -41 11/00/1953 2.3 08115/1985 A Provides water to summer homes. IIIALYM 5,340 12 08/05/1972 7 08/05/1972 .2(2) S IIIALYM 5,320 S lllALYM 5,250 13 09/22/1975 10 1.2(2) M 0 123NRWD 5,280 15 08/2111973 S IIIALYM 5,210 10 12100/1978 45 S IIIALYM 5,200 20 0110111976 M 0 IIIALYM 5,250 45 07/25/1967 S

33 Table 7. Records of wells-Continued

Depth to Use Type Type Date Depth first of of of Location Owner drilled of well opening Finish water lift power (feet) (feet)

(A-7-1) 17bcb-1 White, Donald 09/22/1975 120 104 P H,I S E (A-7-1) 17cba-1 Prier, Peler 1950 300 H,S S E (A-7-1) ISadb-1 Hawks, Monly 10/09/1 976 116 95 S H,I S E (A-7-1) 19aad-1 Dawson, Dale 03100/1972 200 122 P H,I,S S E (A-7-1)19abb-1 West, Bob 06/00/1976 290 no P H,S S E (A-7-1)19acd-1 Finder, Robert 12/02/1971 124 101 P H,S,I S E (A-7-1)19ddb-1 Anderson, Richard 12/10/1971 140 110 PH (A-7-1 )20bab-1 Hogge, Ronald OS/OO/197 I 127 109 P H,I S E (A-7-1 )20dcd-1 Hadfield, Douglas H,I S E (A-7-1)2Ibab-1 Hannum, Thomas OS/IS/l976 125 95 P H,I S E (A-7-1)2Ibbc-1 Pletcher 07/15/1969 SI SI X H,I,S S E (A-7-1 )2Icad-1 Burton, Howard 05/0I/l96S 42 34 PH S E (A-7-1)2Iddc-1 Valley Water Users P (A-7-1)22bcd-1 Wolf Creek Resort 09/00/1972 795 U (A-7-1)22cad-1 Wolf Creek Resort 04/30/1982 400 P (A-7-1)27abc-1 Eden Water Assoc. 08/00/1976 300 160 P P S E (A-7-1)27baa-1 Crandall, Ralph 06/25/1963 395 60 P H,S S E (A-7-1)28adb-1 Holmstron, Dave 11/00/1979 240 220 P H,S S E (A-7-1 )28baa-1 Nipko, Tuck 09107/1970 275 255 P H,I S E (A-7-1)28dbb-1 Chambers, Earl 09/16/1970 S9 89 X H,I S E (A-7-1)28dda-1 Malan, A.B. 06/24/1957 75 U (A-7-1)29acc-1 Bealba, Pete 02/00/1977 300 ISO P H,I S E (A-7-1)29ada-l Pilcher, John OS/20/1974 146 146 X H,I S E (A-7-1)29baa-1 Woorlander, Stanley 1916 60 U (A-7-1)29dbc-1 Thatcher, Ben 300 H,I,S S E (A-7-1)29ddc-1 Hensley, Betty OS/24/1971 51S 117 P I S E (A-7-1)30aad-1 Rich, Steve 09/22/1 980 170 160 P H,I S E (A-7-1)32abd-1 Nordic Valley Water Assoc. P (A-7-1)32dba-1 Nordic Valley Water Assoc. 12/09/1966 193 50 PP S E (A-7-1)32dcd-1 Nordic Valley Water Assoc. 06/12/1963 260 40 P P S E (A-7-I)34aca-1 Carver, David 06/24/1982 144 135 PI S E (A-7-1)34bab-1 Johnson, Dave 07/10/1949 75 65 PU (A-7-1 )34cbb-1 Wolf, Charles 08100/1 974 210 H,S,1 S E (A-7-1 )34ccc-1 Ruskin, Harvey 11/00/1 976 160 140 PH S E (A-7-1)34cda-1 Forest Service 07/02/1961 75 53 PU S E (A-7-1)34dbb-1 Laub, John 05/1 9/1 982 120 120 X I S E (A-7-1)35bbb-1 Eden Cemetery 11/14/1981 160 100 P I S E (A-7-1)35cac-1 Vanscoyk, Robert 20 I C E (A-7-1)35cdd-1 Evergreen Ranch 1932 20 U (A-7-1 )36bdd-1 BAR-B Ranch 06/20/1949 95 65 P H,S,I S E (A-7-1 )36dca-1 Whitehead, Wilford 12/01/1975 117 95 P H,I S E (A-7-3) IOcda-1 Furlong, Ramona 06100/1 978 2S3 243 PH S E (A-7-3)2Ibda-1 Shupe, Don 1981 166 146 PH S E (A-7-3)32bbb-1 Neilsen, H. Eugene 10/0911963 214 100 P U (B-7-1)lbab-2 LDS Church 1968 200 P,I S E (B-7-1)ldaa-1 Tydeck, Robert 09/24/1966 130 110 P H,I S E (B-7-1)ldda-1 Carlsen, Dean 07/01/1970 253 230 P H,S,I S E (B-7-1)12bdc-1 Weber County 09/05/1 975 205 145 PP S E (B-8-1 )36cab-1 Cronquist, Curt 06/08/1977 160 100 P H,I S E (B-8-1 )36dcc-1 Dufree Creek Estates 06/00/1976 332 272 P U

34 Date Specific Altitude water Date capacity Other data of land Water level Discharge discharge (gallons per available Aquifer surface level measured (gallons measured minute per foot WL OW Remarks (feet) (feet) per minute) of drawdown)

IIIALYM 5,180 50 S 0 IIIALYM 5,160 67 12/18/1963 35 12/0011963 S IIIALYM 5,240 30 11108/1976 10 11/0811976 S IIIALYM 5,135 14 03/00/1972 20 .2(2) S 0 123NRWD 5,240 3.1 07/05/1985 50 06/30/1976 0 IIIALYM 5,170 20 12/15/1971 20 12/00/1971 2 (I) S Flows over casing in spring. IIIALYM 5,150 F 01118/1972 36 01118/1972 1.2(2) Flows constantly. IIIALYM 5,120 27 01/00/1972 25 1971 1.7(1) S 5,050 M 0 IIIALYM 5,080 10 10 .1(2) S IIIALYM 5,075 18 0711811969 8 .2(2) S 0 IIIALYM 5,070 18 10/20/1968 19 1.2(1) M 5,100 Eden Hills subdivision. 123NRWD 5,230 3.4 08/07/1984 36 .1 0 I24WSTC 5,240 -4 05120/1982 600 05120/1982 123NRWD 5,120 26.7 08/04/1984 120 .4(24) 0 Secondary water for Eden. IIIALYM 5,110 40 07/03/1963 8.4 08128/1975 S IIIALYM 5,040 70 11/27/1979 35 S IIIALYM 5,020 42 09/15/1970 15 .5(1) S 0 IIIALYM 5,000 24 09125/1970 10 09/00/1970 .5(2) S IIIALYM 4,990 26 20 0712311957 S IIIALYM 5,190 50 02/00/1977 9 02/00/1977 .1(36) S IIIALYM 5,080 4 08/07/1974 10 .2(2) S 0 5,120 S IIIALYM 5,320 S IIIALYM 5,290 50 12/05/1974 50 .3(14) S IIIALYM 5,300 140 15 1.2(1) S 5,440 S Well 3. IIIALYM 5,560 150 1.6(3) Well 2. IIIALYM 5,850 200 1.8(5) Weill. IIIALYM 4,955 20 07/10/1982 25 2.5(1) S 0 IIIALYM 4,975 35 S 300CRSL 4,930 50 08/0011974 30 S 123NRWD 5,230 35.1 08/02/1984 0 112ALYM 4,900 F 07/05/1961 70 35 (I) SA 112ALYM 4,950 35 0512111982 60 M IIIALYM 4,970 10 11117/1981 35 M IIIALYM 4,935 S IIIALYM 4,935 S IIIALYM 4,945 45 S IIIALYM 4,920 70 12/11/1975 S 300CRSL 6,320 240 06112/1978 200 124WSTC 5,960 101.4 07/20/1985 5 0 I24WSTC 5,800 3 11107/1963 30 .3(20) 5,550 M IIIALYM 5,420 15 10115/1966 4 1011511966 <.1 S IIIALYM 5,410 60 08113/1970 10 <.1 S 112ALYM 5,670 145.4 08/03/1984 5 0 Provides water to field school. 400MUTL 5,780 77.5 07/18/1985 45 0 400MUTL 5,620 33.7 07/18/1985 30 06/30/1976 0 A

35 Little recharge results from rainfall when com­ months. Seepage between station 10137500 near the pared to that from snowmelt. During the summer, any valley edge and station 10137600 near Pineview Reser­ precipitation that infiltrates the soil is retained as soil voir was calculated for the water years 1960-64. moisture, and infiltrated water in excess of soil mois­ Discharge and seepage for the South Fork Ogden River ture recharges the aquifer. Thomas (1952, p. 94) between station 10137500 and station 10137600 from observed that recharge to the aquifer occurred only November through February, water years1 1960-64 when more than 1.5 inches ofprecipitation fell on mois­ ture-deficient soils. Average Average discharge discharge Seepage Field measurements indicate that seepage from at station at station to certain reaches of the North Fork Ogden River, Middle Month 10137500 10137600 aquifer Fork Ogden River, and South Fork Ogden River (cubic feet (cubic feet (cubic feet per second) per second) per second) recharges the valley-fill aquifer system. Seepage also is likely from eight small perennial creeks and from all November 35.3 10.6 24.7 ephemeral creeks when they are flowing. December 32.9 13.1 19.8 Measurements on the North Fork Ogden River in January 32.4 16.4 16.0 1985 indicate seepage from the stream to the valley-fill February 36.9 26.1 10.8 aquifer system occurs in the upper reaches. Seepage of about 2.4 cubic feet per second is indicated by the first I Data for February 1962 were not included. two measurements shown in table 4. Actual seepage from the South Fork Ogden Val­ On the Middle Fork Ogden River, all flow for ley to the valley-fill aquifer system may be greater than November through February of water year 1964 was the calculated seepage values because of ground-water lost between station 10137780 and station 10137800 seepage into the stream channel upstream from station (pI. 2). This loss equalled about 3 cubic feet per second. 10137600. The discharge values for February 1962 During the same period in water year 1965, seepage to were not included in the 1960-64 average discharge cal­ the aquifer decreased from 5.1 cubic feet per second in culation because of unusually large tributary inflows November to 1.6 cubic feet per second in February. A for this time of year. net loss of 4.3 cubic feet per second was indicated Seepage from irrigation canals and ditches to the between the upper bridge across the Middle Fork valley-fill aquifer system does not appear to be substan­ Ogden River (site Ml) and the lower gaging station tial in Ogden Valley. Many of the ditches serve as (site M2) for late February 1985 (table 4). drains, particularly around Eden and east ofHuntsville. Seepage from the South Fork Ogden River to the During the summer of 1985, seepage to the aquifer sys­ valley-fill aquifer system was calculated from measure­ tem ofabout 4.0 cubic feet per second was measured for ments made in the summer of 1925 when the water was the Ogden Valley (or Mountain Valley) Canal from the returned to the channel after the streamflow had been diversion structure on the South Fork Ogden River to diverted for several weeks (Browning, 1925, p. 17-20). the tail of the canal reach about 9 miles downstream. On the second day after flow was restored, the entire The seepage occurred near the canal crossing at the flow of about 48 cubic feet per second seeped into the Middle Fork Ogden River (Herbert and others, 1987, p. valley-fill aquifer system within 1 mile. The rate of 7-8). seepage decreased downstream. Water that is diverted from streams and used to Typically during the winter, the South Fork irrigate fields also results in recharge. In a typical sea­ Ogden River is perennial. During the winter of 1933­ son, the water is applied to about 7,000 acres from late 34, the entire flow seeped into the valley-fill aquifer April to early October. Much of the diverted water is system; discharge from the South Fork Ogden River consumptively used or returned to streams, but the into the valley at that time averaged about 35 to 40 excess irrigation water recharges the aquifer over a cubic feet per second (Leggette and Taylor, 1937, p. wide region. 132-133). Most of the bedrock bounding the valley-fill Streamflow records for the South Fork Ogden aquifer system is not permeable except locally where River for November through February indicate that, in fractures and solution channels are present; however, general, seepage to the aquifer decreases during those the cumulative subsurface inflow from the bedrock to

36 the valley-fill aquifer system is large because of the much as 6 feet at this site. The depths ofcompletion for large area ofcontact between the bedrock and the valley these wells are shown in table 7. fill. Therefore, subsurface inflow is a major source of recharge to the valley-fill aquifer system. Hydraulic Characteristics The principal aquifer is recharged primarily by The quantity of water an aquifer can store downward movement of water near the valley margins. depends partly on its thickness. The thickness of the From the analysis of well hydrographs, Thomas (1945, valley-fill deposits (fig. 5) was estimated with a combi­ p. 18-19) determined that snowmelt and part of the nation of electrical resistivity soundings made in 1986 spring runoff infiltrated the principal aquifer along the and well-log descriptions. The Norwood Tuff underlies valley margins and moved toward the center of the val­ the valley-fill deposits throughout most of the valley ley. Some recharge moving through the principal aqui­ and has a resistivity that sharply contrasts with that of fer is rejected before it reaches the confined part of the the overlying valley-fill deposits. The valley-fill depos­ system; rejected recharge probably discharges to its are more than 750 feet thick along the east-bounding stream channels or recharges the shallow water-table fault zone northeast of Huntsville. The deposits also aquifer that overlies the confined part of the principal are relatively thick near Liberty where they appear to be aquifer. underlain by carbonate rocks. Locally near the Ogden well field, water from the Aquifer tests of the valley-fill aquifer system Pineview Reservoir probably recharges the confined were conducted during this study because results from aquifer. In this area, the vertical hydraulic gradient is previous aquifer tests were not available. A long-term downward because of the drawdown that results from aquifer test of the confined part of the principal aquifer pumping. was conducted using wells in the Ogden well field. Well (A-6-1)1] cab-3 was pumped for 4 days and Movement allowed to recover for 4 days. Water-level measure­ ments were made in the pumped well and in seven The potentiometric surface of the principal aqui­ observation wells during the pumping and recovery fer during June 1985 is shown in figure 11. The direc­ periods. Three similar transmissivity values were tion of ground-water flow generally parallels the land obtained from the test. Storage coefficient values could surface; water flows from the valley margins toward not be determined because soon after pumping started, Pineview Reservoir in the southern part of the valley. boundary effects were observed in the water-level The hydraulic gradient ranges from about 15 feet per response in the observation wells. mile near Pineview Reservoir to about 80 feet per mile Results from the aquifer test are as follows: in the northern part of Ogden Valley. Characteristics obtained from an aquifer test of the confined Vertical head gradients have been detected part of principal aquifer, October 3-10, 1985 throughout the valley-fill aquifer system. Generally, [Boundary: D, discharge image; R, recharge image] gradients are downward in the recharge areas and upward in the discharge areas. Near the recharge area Location Distance Transmissivity Distance from along the upper South Fork Ogden River, a downward from (feet pumped well vertical head gradient in the unconfined part ofthe prin­ pumped well squared to boundary cipal aquifer is evident by comparing water levels in (feet) per day) (feet) wells (A-6-2)21 abc-I and 2 (fig. 12). The water level (A-6-1) IOaac-I 3,000 No drawdown in the deeper well [(A-6-2)2Iabc-2] is as much as 10 (A-6-1)lOdda-l 2,800 Indeterminate 4,900 D 6,300 D feet lower than the water level in the shallower well 9,900 R [(A-6-2)21 abc-I]. (A-6-l)llacb-1 1,600 No drawdown (A-6-l)llcab-l 125 83,000 530 R 5,600 D A downward vertical head gradient in the con­ (A-6-l)llcab-3 79,000 fined part of the principal aquifer is evident near the (A-6-l)llcba-2 475 87,000 4,500 D Ogden well field by comparing water levels from a (A-6-1)lldcd-2 3,050 Indeterminate 5,300 D 5,800 D multiple-completion well at (A-6-l)llcab-1 (fig. ]3). 6,700 D 6,800 R (A-6-2)18bad-1 11,300 Indeterminate 30,000 D 38,000 D During the low stage of Pineview Reservoir, the differ­ ence in water levels in the shallow and deep wells is as

37 111°52'30" EXPlANATION I -- 5,000 -- Potentiometric contour of 41°22'30"- principal aquifer - Shows altitude at which water level would have stood in tightly cased wells, June 1985. Contour interval, in feet, is variable. Datum is sea level

111°45' I

R.1 W. R. 1 E.

1. 7 N.

T.6 N.

l .( \ /

i

R.1 E. R.2 E. Base from U.S. Geological Survey Ogden, 1: 100,000, 1976

o 2 3 MILES I I I I I o 2 3 KILOMETERS

Figure 11. Potentiometric surface of the principal aquifer, June 1985.

38 2.5

5.0

7.5 (A-6-2) 18dad-2

10.0 JFMAMJJA SON DJFMAMJJA SON DJFMAMJJA SON D 1984 1985 1986

w 7.5 () a:Lt 10.0 ::::> CI) o z 12.5 :5 (A-6-2)21 abc-1 :> 15.a L-L--'--'--'---'~--'--'--'---'---'--'---'-"---"--'--'--'--'~--'--'--'---'---'--L--'--"---"--'--'---'--'---'----'--' o JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND u:J 1984 1985 1986 CD ~ W w 5 u. Z ....i 10 w > ~ 15 a: w ti: 20 ;:: (A-6-2)21 abc-2 25 JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

0.5

1.0

1.5 (A-6-2)28aaa-1

2.0 JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

Figure 12. Water level in wells in the upper South Fork Ogden River valley, 1984-86.

39 4,900

4,890

4,880 - (A-6-1)11acb-1

4,870 JFMAMJJA SON 0 JFMAMJJA SON 0 JFMAMJJA SON 0 -J ~ 1984 1985 1986 w -J « w (J) w 6 4,890 CD« I­ w 4,880 LLW Z 4,870 ..i (A-6-1 )11 cab-1 Deep well w ~ 4,860 JFMAMJJA SON 0 JFMAMJJA SON 0 JFMAMJJA SON 0 a: 1984 1985 1986 w ~ ~

4,900

4,890

4,880 (A-6-1 )11 dcd-2

4,870 L.-..L--'--'--'---.J...-l---L.--L.---L-..I--L....-J.--'---'---'--'----'----'----,---,--.L.-.....J---L.--'---'-..I--L...... L---'--'--'---.L.-.....J---'---L.--' JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

4,910 ~t:i-J !:!:!ww >LL> 4,900 z--Jwzw a..a:w- -« LLO(f) 4,890 Q>w wa:> (,)wQ 4,880 «(f)CD PINEVIEW RESERVOIR (f)a:I-'w« 4,870 J FMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

Figure 13. Water level in wells near the Ogden well field and Pineview Reservoir, and stage of Pineview Reservoir, 1984-86.

40 Drawdown data were analyzed from the observa­ Transmissivity values determined from 1-hour aquifer tests tion wells; recovery data were analyzed from the [Transmissivity: First value delermined from early part of aquifer test; pumped well. The early-time data, before boundary second value from laler part of aquifer test] effects occurred, were analyzed with the straight-line solution to the Theis equation (Lohman, 1972, p. 23­ Location Transmissivity Time of Discharge (feet boundary (gallons 27). The apparent transmissivity determined from the squared effect per observation wells increased with increased distance per day) (minutes) minute) from the pumped well. The apparent increase in trans­ (A-6-2) 15acb-l 140; 110 6 33 missivity indicated that leakage was occurring through (A-7-I )8cad-1 40; 15 20 16 the confining layer. Thus, the transmissivity of about (A-7-1)19aad-1 310; 50 14 23 79,000 feet squared per day determined from the (A-7-I )28baa-1 30; 15 13 8.2 pumped well probably is the most representative value (A-7-1 )34aca-1 20; 480 7 13 for the aquifer.

The boundary effects that occurred during the The confining layer between the principal aquifer and the shallow water-table aquifer in Ogden Valley aquifer test also were interpreted. The distances to the extends over an area of about 10 square miles in the discharge image and to the recharge image were esti­ southern part of Ogden Valley (Leggette and Taylor, mated with the image-well theory (Lohman, 1972, p. 1937, pI. 36). Leggette and Taylor (1937, p. 110) 59-61). An impermeable boundary that coincided with described samples of the confining layer as thin layers the concealed fault zone on the west side of the valley of dense, sticky, putty-like clay and silt, usually gray­ at the mouth of Ogden Canyon (pI. I) was defined. An ish-blue and brown. Lofgren (1955, p. 81) indicated additional impermeable boundary oriented in a north­ that the confining layer commonly is silt and fine sand. west direction was defined on the east side of the well Maximum thickness ofthe layer is about 100 feet; aver­ field. This boundary was interpreted as a previously age thickness is about 70 feet (Thomas, 1945, p. 8). unknown fault (pI. I). The two observation wells that The stream channels that were inundated by Pineview did not show any drawdown are on the opposite side of Reservoir were entrenched about 25 feet into the con­ the faults from the pumped well. The coincidence of fining layer. faults with impermeable boundaries indicates that flow Laboratory tests on samples of the confining through the aquifer is retarded by the faults. layer indicated hydraulic-conductivity values of less than 0.013 foot per day (Leggette and Taylor, 1937, p. Several short-term aquifer tests were conducted 137). Reservoir-bed seepage measurements made in on five different wells, each of which was pumped for July 1986 with a method described by Lee (1977) indi­ I hour. The drawdown in each pumped well was ana­ cated that vertical hydraulic conductivity ranged from lyzed with the straight-line solution to the Theis equa­ 0.01 to 0.04 foot per day. These values are typical for tion (Lohman, 1972, p. 23-27). All of the short-term silt beds and indicate that the layer isa leaky confining aquifer tests apparently were affected by drainage from layer. the gravel pack in the well annulus. In the following Along the now-inundated stream channels, the table, the first transmissivity value listed was deter­ confining layer is relatively thin, and upward leakage to mined from the early part of the test, and the second Pineview Reservoir may be substantial. Before the res­ value was determined from the later part of the test. ervoir was constructed, springs and seeps were com­ The transmissivity values have not been adjusted for mon in the stream valleys along the contact of the partial penetration and perforated interval of the well. confining layer and the overlying sand layer comprising the shallow water-table aquifer (Leggette and Taylor, Specific-capacity values determined from the 1937, p. 136). well discharge and water-level declines given on well­ The water level in well (A-7-1)34aca-l, com­ drillers' reports submitted to the Utah State Engineer's pleted at a depth of 144 feet, does not seem to be Office are shown in table 7. The specific-capacity val­ affected by the presence or absence of water in a nearby ues ranged from less than 0.1 to 125 gallons per minute canal. Thus, the confining layer may exist farther north per foot of drawdown. than is indicated in previous reports, to about 1 mile

41 northwest of Eden in the North Fork Ogden River Discharge drainage. Ground-water discharge occurs by seepage to streams, springs, drains, and Pineview Reservoir; by Storage well discharge; and by evapotranspiration. Each of these is important in the water balance during some part Historic changes in storage, as indicated by long­ of the year. term water-level measurements, can be attributed pre­ Few data are available for the water discharged dominately to man-induced changes in the hydrologic naturally from the aquifer to the streams in Ogden Val­ regime. The most prominent change is the impound­ ley. Spring Creek is east ofHuntsville along the margin ment of water in Pineview Reservoir. Filling ofthe res­ ofthe confining layer that overlies the principal aquifer, ervoir began in 1936, and capacity was reached in and the creek derives most of its flow from ground 1938. In 1957, Pineview Reservoir dam was raised 30 water. The average flow of Spring Creek ranged from feet. Maximum storage capacity in the enlarged reser­ 7.0 to 9.4 cubic feet per second from November voir was reached in 1962. These changes mostly through February of water years 1958-65. This flow affected water levels in the confined part of the princi­ likely represents ground-water discharge to the creek. pal aquifer. The long-term water-level rise in wells near the reservoir averaged 10 to 15 feet. Seasonal Observations of streamflow in Bennett Creek by changes in water levels typically were 15 to 25 feet Browning (1925) indicated that the creek was dry from (figs. 14, 15, and 16). July until sometime in the late fall. Now, the creek flows perennially, with much of the summer flow prob­ In the upper South Fork Ogden River valley, ably derived from irrigation return water. A flow of8.9 water levels fluctuated a maximum of about 26 feet in cubic feet per second was measured in February 1985 1986 (fig. 17). In the North Fork Ogden River valley, just upstream from the confluence of Bennett Creek water-level fluctuations were as much as 15 feet in 1985 with Bally Watts Creek (table 4). Part of this flow rep­ (fig. 18). The lowest ground-water levels near the resents discharge from the Wasatch Formation. major stream channels occurred in the late fall as Liberty Springs, (A-7-1) 19dbc-S I (table 6), and streamflow continued to be diverted for irrigation (fig. 19). Liberty Spring Creek derive most of their flow from ground-water seepage, but long-term discharge has not The water-level rise in the principal aquifer from been measured. Liberty Spring Creek was measured in late February to early June 1985 is shown in figure 20. February 1985 just above its confluence with the North The largest water-level increases in the principal aqui­ Fork Ogden River. A flow of 13 cubic feet per second fer occurred beneath Pineview Reservoir, in the North was measured (table 4). Fork Ogden River valley near Liberty, and east of The original Ogden artesian well field consisted Huntsville. The large water-level changes in the con­ of46 flowing wells located just north of the juncture of fined part ofthe principal aquifer do not represent large the three forks of the Ogden River. The first well was volume changes because of the small storage coeffi­ drilled in 1914. The artesian well field was inundated cient. The storage coefficient ofthe confined part ofthe by Pineview Reservoir in 1936 but continued to be used principal aquifer is assumed to be 0.0001. The specific until 1970. Because of contamination problems from yield of the unconfined part of the principal aquifer is iron bacteria entering either the underwater pipeline or assumed to be 0.10. Because of water-level changes in the wells, the artesian well field was abandoned, and six the spring of 1985, the quantity of water added to stor­ replacement wells were drilled on the nearby shore of age in the entire unconfined part ofthe principal aquifer the reservoir. The wells at the new location have to be was about 8,900 acre-feet. The quantity ofwater added pumped to yield water. Pumpage from the Ogden well to storage in the confined part of the principal aquifer field from 1970 to 1985 averaged 10,290 acre-feet per during this same period was about 8.5 acre-feet. year or about 14.2 cubic feet per second. Water levels in the shallow water-table aquifer Many wells in Ogden Valley are used for domes­ typically fluctuate 10 to 15 feet during the year (fig. 21). tic purposes and for stock water. Lately, many new The quantity of water added to storage in the spring of wells have been permitted in Ogden Valley for individ­ 1985 in the shallow water-table aquifer is estimated to ual domestic use. Wells also are used by small commu­ be 4,600 acre-feet. nity systems to provide water to individual housing

42 w 20 0 it a: ::::> Cf) 40 Clz (A-6-1)11dcd-1 :5 MEASURING POINT ALTITUDE 4,881 FEET ~ 60 LO 0 LO 0 LO 0 (t) " 0> 0> 0> 0> W T"" T"" (() I- W w LL 20 Z ..1 30 w >w 40 ....J a:: 50 w ~ 60 ~ (A-6-1 )11 dcd-2 70 MEASURING POINT ALTITUDE 4,915 FEET 80 LO 0 LO 0 LO LO co co t-- t-- 0> 0> 0> 0> 0> T"" T"" T"" T"" T""

Figure 14. Water level in wells in the principal aquifer near Pineview Reservoir, 1935-61.

43 0 (A-6-1 )11 cab-1 -~UJ .....JOO Shallow well ~.....JLf 25 UJUJa: .....J CO ::> a:1-(J) UJUJ ~~ZO 50 ~z

75 0 LO 0 LO 0 LO 0 LO LO CD CD t-- t-- co m m m m .....m m m

+20 ..-~ w (A-6-1)12aad-1 u:J ~:±O +10 >0UJ.....J~a:Lf .....JUJO::> Land surface a::COCO(J) 0 UJI-

-20 0 LO 0 LO 0 LO 0 (Y) (Y) ..;t ..;t LO LO co m .....m .....m m .....m m..... m.....

(A-6-2)18bad-1

~ NO'~ _

coLO m.....

Figure 15. Water level in wells in the principal aquifer near Pineview Reservoir, 1932-84.

44 4,910

4,900

4,890 (A-6-1)1baa-1

4,880 L-..--,-~~~~~---,-----,--L.-.i--,---,----,--,---,--,--,--,--~~-----L~--,--,------,---,-~-,---"--,,--,---,--J ....J JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND UJ > 1984 1985 1986 UJ ....J « UJen UJ >o 11l« t­ UJ UJLL Z

....J (A-6-1 )1Odda-1 UJ >UJ ....J 4,860 JFMAMJJA SON DJFMAMJJA SON DJFMAMJJA SON D a:: 1984 1985 1986 UJ t;: ~

4,880 (A-6-1 )13cdd-1

4,870 L....L--'-~~~~~---'-----'--'----'---'----'-----'--'---'--'-~-'---'----''---'----l..---'--~~--'-~~-'----'--'-~-J JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

4,910 ~t:i....J !!!UJUJ >LL> 4,900 UJZUJ z_....J - -« o.a::UJ 4,890 LLOen O>UJ UJa::>

Figure 16. Water level in wells in the principal aquifer, and stage of Pineview Reservoir, 1984-86.

45 20

w () 30 LE a: ::J (j) 0 40 Z <{ -.J (A-6-2)15acb-1 5: 50 0 JFMAMJJASONDJFMAMJJASON DJFMAMJJASON 0 -.J w 1984 1985 1986 en f-w w LL 0 Z -.Jw 10 > W -.J 20 a: w ~ 30 ~ (A-6-2)15cdb-1 40 JFMAMJJASONDJFMAMJJASONDJFMAMJJASON 0 1984 1985 1986

Figure 17. Water level in wells in the upper South Fork Ogden River valley, 1984-86.

46 5

10

15

20 (A-7-1 )8cad-1

w 25 L---'.--'--'-__"____'___'---'--'--__'__-'----'C---!.--'--~--'--'---'-____'_____'_--'--"'----'____'_----I..--'---'--<------.L--'---'---'--"'----'---'----'-_' () JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND Lt 1984 1985 1986 a:: :::> (J) o z j

~ 5 .--J W co I­ W 10 W LL Z (A-7-1 )20dcd-1

.--J 15 l-...L____'_-'--~__"____'___'____'___'__'___'__..l._L...... L____'__'_~_'__L_...<___'_____'___'__I.__'_____'____'___'_____'___'___'__L_...<____'_____'___J ~ JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND ~ 1984 1985 1986 a:: w

~ 35.0 ,...,-----.--,------r--r-T---.----.---.---.,...--,r-,-----'--'--'-""'---'--'----"'-r-T---.----.--.--,---,r--r----.--,------r--r-T--r----r--;

37.5

40.0 (A-7-1 )34dbb-1

JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

o

-10

(A-7-1 )35bbb-1

JFMAMJ J ASONDJFMAMJ J ASONDJFMAMJ J ASOND 1984 1985 1986

Figure 18. Water level in wells in the North Fork Ogden River valley, 1984-86.

47 5.0

7.5

(A-7-1)1 bab-2

~ 10.0 JFMAMJJA SON DJFMAMJJA SON DJFMAMJJA SON D ~ 1984 1985 1986 ::J CJ) o z 5.0 ,..--,--,---r--r-""---'--'r--T----r-r--.---,--r-T--,-----r--r--r--,--,r--r----r---,--,--r-...---T--r---,--r-""--'--r--T--r--, ::5 ~ -l 7.5 W co ~ w 10.0 u.. z (A-7-1)7dba-1

.J"w 12.5 l.-.J.---,--",---,---,--",--,---,---'--,---'--..L--L...... L--'--'---'--.J--",--,---'---'--L---l..--'---'L...... L--'--'---'---'--"'--'---'---'--l > JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND ~ 1984 1985 1986 a::: w ~ ~

5

10 (A-7-1)21cad-1

JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND 1984 1985 1986

Figure 19. Water level in wells in the North Fork Ogden River channel, 1984-86.

48 111°52'30" EXPlANATION

--10-- Line of equal water-level rise­ 41°22'30"- Interval 5 feet

111°45' I

R.1 W. R.1 E.

T. 7 N. T.6 N.

41°15'-

l )

R. 1 E. R. 2 E. Base from U.S. Geological Survey Ogden, 1:100,000, 1976

o 2 3 MILES I I I i o 2 3 KILOMETERS

Figure 20. Water-level rise in the principal aquifer from late February to early June 1985.

49 3 6 9 12 15

18 (A-6-1)1aaa-1 UJ () 21 it J F M A M JJ A S 0 N D J F M A M J J A S 0 N D a: 1970 1971 ::::> (/) 0z « 3 ...J s: 6 0 ...J 9 UJ (0 f- 12 UJ UJ 15 LL z 18 (A-6-2)18dbb-1 ...i UJ 21 > J F M A M A N D M N D UJ JJ S 0 J F M A JJ A S 0 ...J 1970 1971 a: UJ t:c s: 3 6 9 12 15 18 (A-7-1 )35cdd-1 21 J F M A M JJ A S 0 N D J F M A M J J A S 0 N D 1970 1971

Figure 21. Water level in wells in the shallow water-table aquifer, 1970-71. (Data collected by V. Doyuran.)

50 tracts. There may be as many as 2,000 small-yield was shut offas a result ofa U.S. Bureau ofReclamation wells in the valley, although it is not known how many plugging program. actually are used. The greatest concentration of indi­ Because the area inundated by Pineview Reser­ vidual wells is east of Huntsville. voir is completely underlain by the confining layer, the early perception was that hydraulic connection between Crops, natural phreatophytes, and other vegeta­ Pineview Reservoir and the confined aquifer did not tion transpire water. Crops grown in Ogden Valley exist (Leggette and Taylor, 1937, p. 143-144). The include alfalfa; spring grains (wheat, barley, oats); observed effect of Pineview Reservoir on water levels com; and grass pasture. Major phreatophytes are cot­ was attributed to mechanical loading of the confined tonwoods, willows, and cattails. Other vegetation part ofthe principal aquifer resulting from the weight of includes big sagebrush, gamble oak, and various surface water in the reservoir. Water levels at the max­ grasses. The area covered by naturally occurring imum springtime level in well (A-6-1)12aad-l phreatophytes and subirrigated cropland is about 4,100 increased about 14 feet shortly after the initial filling of acres. Of this area, 1,450 acres has more than a 50-per­ the reservoir in 1938 (fig. 15). Maximum water levels cent density of cottonwoods and willows. Cotton­ in well (A-6-2)18bad-l increased about 10 feet after the woods, willows, and cattails consume an average of5.1 reservoir filled to its expanded storage capacity in 1962. feet of water per year; grasses and small phreatophytes consume an average of 2.1 feet of water per year (Feth It is now thought that loading had an initial effect and others, 1966, p. 69). These rates were determined on the water levels in the principal aquifer and that for the East Shore area of Great Salt Lake assuming upward leakage to Pineview Reservoir from the con­ 100-percent density. fined part ofthe principal aquifer controls ground-water levels. Leakage through the confining layer is driven The annual consumptive use in Ogden Valley by by the difference in water levels between Pineview the phreatophytic vegetation and subirrigated cropland Reservoir and the confined part ofthe principal aquifer. was determined using the above rates and assuming A seepage rate to Pineview Reservoir ranging from 100-percent density for grasses and associated plant 0.17 to 0.20 foot perday was measured at three sites (pI. communities and 80-percent density for cottonwoods 2) by use of seepage meters installed underwater on the and willows. The estimated annual consumptive use is lakebed in July 1986. The seepage was assumed to be about 11,500 acre-feet. Doyuran (1972, table 13) esti­ moving upward through the confining layer in the bot­ mated annual evapotranspiration by crops and vegeta­ tom of Pineview Reservoir. tion at 20,000 acre-feet. Most water movement is upward into Pineview Reservoir, but some downward leakage may occur near Effects of Pineview Reservoir the current Ogden well field because water levels in the wells usually are below the stage ofPineview Reservoir After its construction in 1936, Pineview Reser­ (fig. 13). voir affected the ground water of Ogden Valley, espe­ cially in the confined part of the principal aquifer. The Water Quality southern part of Ogden Valley was marshy before con­ struction of the dam. All leakage from the principal Selected drinking-water standards set by the U.S. aquifer was upward to the land surface and either was Environmental Protection Agency (USEPA) (1986) for consumed by evapotranspiration or ran off in stream human health are: channels. After the dam was completed, upward leak­ Dissolved solids concentration should not exceed 250 age from the principal aquifer flowed into the reservoir milligrams per liter for chlo­ and was released downstream or evaporated. The nat­ ride and sulfate ural discharge of ground water from exposures of the Iron should not exceed 300 micro- valley-fill deposits in the southern part of Ogden Valley grams per liter was captured by Pineview Reservoir. Natural discharge before completion of the reservoir was estimated to be Manganese should not exceed 50 micro- less than 5 cubic feet per second (Leggette and Taylor, grams per liter 1937, p. 139). Flowing-well discharge in the area inun­ Nitrate and nitrite should not exceed 10 milli- dated by the reservoir, except for the Ogden well field, grams per liter

51 Fluoride should not exceed 1.4 to 2.4 for MBAS were used to determine if ground-water milligrams per liter depend­ seepage from the base of hillsides on the north and ing on air temperature south sides ofHuntsville originates, in part, from septic pH should be between 5.0 to 9.0 tank outflow. The concentration of surfactants in untreated wastewater would be about 8 to 10 milli­ Fecal coliform bacteria should not exceed 1count (or grams per liter (Duthie, 1972, p. 341); however, the colony) for every 100 MBAS values of 0.03 milligrams per liter for seepage milliliters of water samples indicate that little of the seepage is derived Analyses of water samples from wells in the val­ from septic tank outflow. ley-fill aquifer system are shown in table 8 and analyses from springs are shown in table 9. Water quality ofthe Water from two wells sampled by Doyuran samples collected in 1985 is diagrammatically shown (1972) had a concentration of nitrate in excess of the on plate 2. Few water samples have been collected in USEPA recommended limit of 10 milligrams per liter. Ogden Valley by the U.S. Geological Survey since the One sample was from a shallow well southeast ofEden 1950's. In 1971, Doyuran (1972) collected and ana­ and the other was from a well south of Liberty. Water lyzed water samples. In general, dissolved-solids con­ from wells sampled by Doyuran (1972) near well (A-6­ centration ofwater in the valley-fill aquifer system does 2)6dad-l, which was sampled for this study, had ele­ not exceed 350 milligrams per liter, and most of the vated nitrate concentrations but did not exceed 10 mil­ water is a calcium-bicarbonate type. Wells that have ligrams per liter. The large nitrate concentration in other than a calcium bicarbonate type water are (A-6­ water from the well southeast ofEden could be derived 2)7ddb-1 and (A-7-1)28baa-1, which have a calcium­ from chemical fertilizer because water from that well sodium bicarbonate type water; (A-7-1 )29ada-1, which did not show a high coliform count; however, unsatis­ has a calcium-magnesium-bicarbonate type water; and factory counts of coliform were found by Doyuran (A-6-2)21acd-l and (A-7-l)8cad-1, which have a cal­ (1972) in water from the well south of Liberty and in cium-magnesium-sodium-bicarbonate type water. water from the wells near well (A-6-2)6dad-l. Generally, ground water in the North Fork Ogden Water that has a pH value of less than 7.0 may River valley is characterized by small dissolved-solids cause pipe corrosion and solubility of trace elements concentrations. Slightly more mineralized ground from natural sources into the water. Water samples water is present in the Middle Fork Ogden River and from two wells, (A-7-1)7dba-1 and (A-7-l)17bcb-1, South Fork Ogden River valleys. Analyses by Doyuran had pH values of less than 7.0, which indicate an area (1972) generally correspond with this distribution. where the water recharging the aquifer is slightly acidic. Larger-than-typical concentrations of some The water type shown for each analysis in table 8 trace elements may occur in water in this area because was determined from values converted from the actual trace elements have greater solubility at small pH val­ concentrations of each ion, in milligrams per liter, to a ues. However, iron and manganese, the only trace ele­ value in milliequivalents per liter. This conversion ments analyzed for in this study, were not detected in makes all of the ions chemically equivalent by adjust­ unusually large concentrations. The concentration of ing for different molecular weights and electrical dissolved iron approaches 300 micrograms per liter in charges. More than 50 percent of a single cation or a two wells, (A-6-2)28aba-1 and (A-7-l)7dba-l, but does single anion, in milliequivalents per liter, indIcates pre­ not exceed the USEPA recommended limit. dominance ofthat ion; otherwise, percentages for each of the predominant cations and anions are added Because snowmelt recharges the aquifer, the pH together until the combination is greater than 50 per­ ofsnow in the valley was measured at three locations in cent. January 1985. Cores that were 2 inches in diameter and about 3 feet long were taken from the snowpack at least Analyses for nitrate are shown in tables 8 and 9. 500 feet from any road. The snow was melted slowly Water from one well, (A-6-2)6dad-l, had a nitrate con­ in sealed tubes for 2 days before the pH measurement centration that exceeded the USEPA standards for was taken. The specific conductance of all snowmelt drinking water. samples was below detection on the conductance meter Analyses for MBAS (Methylene-Blue Active which had a minimum scale reading of 1.0 microsie- ' Substances), which is an indicator of manmade surfac­ men per liter. The pH values of the snowmelt samples tants or sudsing agents, are shown in table 9. Analyses are as follows:

52 pH values of snowmelt tions. Values in the budget were used for data entry and for calibration of a ground-water model that simulated flow in the valley-fill aquifer system. Details of the Sample pH value General location (standard site model are described later in this report. Values deter­ units) description mined on a monthly basis for each component of the water budget can vary from year to year, so the values Lat.41°21'27"N., 5.2 Near well (A-7-1) 7dba-1 presented in this report are unique for the indicated time long. 111° 52' 47" E period. The budget values will vary because of cli­ Lat. 41° 19' 22" N., 6.7 Near well (A-7-1 )27baa-1 matic conditions such as the time and duration ofsnow­ long. 111°49' 38" E melt, the summer temperature, and the quantity of Lat. 41 0 14' 01" N., 6.2 Near well (A-6-2)28aaa-1 precipitation. long. 111 0 43' 26" E Recharge

According to Messer and others (1982, fig. 2), the The valley-fill aquifer system is recharged from pH value of5.2 is low for snowmelt in the region. This various sources. Each source was analyzed separately pH value was determined for the snowmelt sample col­ to provide detailed analysis of the ground-water-f1ow lected near well (A-7-1)7dba-1, which yielded the system. smallest pH value of all samples from wells (table 8). The temperature of all ground-water samples Precipitation exceeded 7.0 °C, which is about the annual mean air temperature for Ogden Valley and the temperature to Recharge from snowmelt occurs during the which shallow ground water usually equilibrates. spring. In 1985, the snowmelt occurred from late Feb­ Ground water from well (A-6-2)16bad-1 had a temper­ ruary through early April. It was assumed that 33 per­ ature of 14.0 °c (table 8). This well is in the area where cent of the total snowpack recharged the aquifer. Doyuran (1972) measured the highest water tempera­ Recharge from rainstorms in 1985 occurred dur­ ture. The elevated temperatures indicate deep circula­ ing October to December. Recharge from rainstorms tion of ground water in the valley-fill aquifer system. was assumed to occur when the total rainfall in a storm Because the highest temperatures are along the pro­ exceeded 1.5 inches, the threshold value determined by jected east-bounding fault zone, it is possible that Thomas (1952, p. 74). It was assumed that 33 percent upwelling of warm water from the bedrock along the of the net rainfall recharged the aquifer. fault is contributing to the elevated water temperatures The areal distribution ofrecharge from snowmelt in the valley-fill aquifer system. and rainstorms was based on the contours showing nor­ Iron bacteria in Ogden wells was first recorded in mal annual precipitation (pI. 1). The estimated rates of 1951, but a sudden worsening of the problem occurred recharge during various periods are shown in table 10. in 1964 (Doyuran, 1972). At that time, the artesian well field was located under Pineview Reservoir and was Irrigation and Irrigation Distribution Losses inaccessible for periodic treatment, so the wells were plugged and abandoned. Replacement wells were Irrigated acreage in Ogden Valley was mapped drilled nearby above the level of the reservoir. from high-altitude, infrared aerial photographs taken in 1981. The mapping was field checked twice in 1985. WATER BUDGET FOR THE VALLEY-FILL During the May-July irrigation season, about 7,000 acres were irrigated. The irrigated acreage declined to AQUIFER SYSTEM about 6,400 acres in August when the small grains were A periodic water budget of all recharge to and harvested. discharge from the valley-fill aquifer system was pre­ All of the irrigation water is derived from sur­ pared for mid-February 1985 through January 1986 face-water sources and springs, but the method ofwater (table 10). The time interval was divided into 12 peri­ application and the consequent recharge potential vary ods that were about 30 days in duration. The budget substantially. Pressurized side-roll and hand-pipe provided estimates of seasonal variations in recharge sprinkler systems and ditch and field-flooding systems and discharge that are large compared to annual varia- are used. It is assumed for the preparation of the water

53 Table 8. Chemical analyses of water samples from wells

IuS/em, microsiemens per centimeter at 25 degrees Celsius; "c, degrees Celsius; mg/L, milligrams per liter; Ilg/L, micrograms per liter; -, no data;

Location: See figure 2 for description of data-site numbering system. Sampling method, codes: 4040, submersible pump; 4090, jet pump; 8010, turbine pump.

Flow Solids, rate, Spe- Hard- sum of Magne- instan- cific Hard- ness, Alka- constit- Calcium, sium, Sodium, Date taneous conduct- pH Temper- ness noncar- Iinity, uents, dis- dis- dis- of (gallons ance (stand- ature (mg/L bonate lab dis- solved solved solved Location sample per (IlS/cm) ard (DC) as (mg/L as (mg/L as solved (mg/L (mg/L (mg/L minute) units) CaC03) CaC03) CaC03) (mg/L) as Ca) as Mg) as Na)

(A-6-1) Idad-I 09-13-85 6.2 185 7.2 12.0 88 5 83 100 27 5.1 4.0 (A-6-1)llcab-3 10-06-85 2,300 320 7.1 9.0 150 20 129 170 43 10 12 (A-6-1)lldbd-1 09-17-32 100 150 30 7.3 II (A-6-1)lldbd-2 09-24-32 30 160 210 47 10 14 (A-6-1)lldbd-3 10-12-32 250 300 73 17 7.2

(A-6-1)lldcd-2 11-04-55 180 415 7.3 9.0 210 16 230 55 17 6.3 (A-6-1)12aad-1 10-12-32 72 210 13 9.5 47 06-17-53 570 7.5 11.0 180 18 320 46 16 49 (A-6-1 )23adb-1 04-04-60 5.0 780 9.4 13.5 10 0 500 4.0 <.1 1190 04-06-60 175 760 8.8 0 0 510 <.1 <.1 1195

(A-6-2) 6dad-1 09-03-85 18 540 7.0 10.5 240 75 163 270 69 16 14 (A-6-2) 7bcc-1 09-03-85 9.0 390 7.8 12.0 160 9 151 250 46 II 22 (A-6-2) 7ddb-1 09-03-85 II 455 7.5 10.5 170 0 181 260 48 II 35 (A-6-2) 8ddb-1 09-03-85 16 360 7.1 9.5 180 7 171 200 50 13 7.3 (A-6-2)14bbd-1 09-13-85 9.0 435 7.6 9.0 210 25 187 240 57 17 14

(A-6-2)15acb-1 08-21-85 31 470 7.7 12.0 220 27 195 260 61 17 15 (A-6-2)15cdb-1 09-04-85 27 340 7.9 8.0 180 10 171 190 51 13 4.8 (A-6-2)16bad-1 09-03-85 5.8 440 7.6 14.0 220 28 191 250 63 15 10 (A-6-2)17cca-1 08-29-85 7.8 370 7.8 9.0 190 14 176 210 53 14 7.2 (A-6-2)17dac-1 09-03-85 9.5 355 7.5 11.0 190 15 173 200 52 14 5.6

(A-6-2)l8bad-1 11-30-55 43 415 7.5 10.0 200 0 240 54 15 <13 (A-6-2)2Iacd-1 09-03-85 6.7 590 7.7 10.0 210 34 172 330 53 18 43 (A-6-2)28aba-1 09-17-85 14 315 7.1 11.0 150 5 140 180 40 II 8.6 (A-7-1) 7dba-1 09-05-85 9.0 140 6.7 11.0 63 II 52 84 18 4.5 3.6 (A-7-1) 8cad-1 08-29-85 18 190 7.3 11.0 73 0 73 110 18 6.8 12

(A-7-1)17bcb-1 09-05-85 5.1 155 6.8 10.0 72 12 60 93 21 4.7 3.9 (A-7-I)l9aad-1 08-26-85 23 365 7.8 9.0 180 13 170 200 57 9.9 5.4 (A-7-1)20dcd-1 09-05-85 4.6 280 7.5 9.0 150 24 123 160 44 8.9 5.4 (A-7-1)2Ibbc-1 09-05-85 7.7 245 7.4 9.5 110 12 96 150 32 6.7 9.1 (A-7-1)28baa-1 08-20-85 8.2 280 8.3 12.0 90 0 115 200 23 8.0 23

(A-7-1)29ada-1 09-13-85 6.8 240 7.2 11.0 100 6 94 150 24 9.7 13 (A-7-1)34aca-1 08-22-85 14 240 7.8 10.0 110 12 94 130 29 8.2 6.9

I Sodium plus potassium.

54 <. constituent concentration less than indicated detectable limits1

Nitro- Nitro- Potas- Chlo- Fluo- Silica, gen, gen, Manga- Sam- sium, Sulfate, ride, ride, dis- Nitrate, N02 +N03 Iron, nese, piing dis- Bicar- Car- dis- dis- dis- solved dis- dis- dis- dis- method, Water solved bonate bonate solved solved solved (mgIL solved solved solved solved codes type (mg/L (mg/L (mg/L (mgIL (mg/L (mgIL as (mgIL (mg/L (I!g/L (l!gIL as K) as HC03 as C03) as 504) as CI) as F) Si02) as N03) as N) as Fe) as MN)

0.9 4.6 3.6 0.1 6.5 0.26 19

1.2 230 0 12 12 .1 10 2.7 <10 4.3 50 7 32 61 .4 4.8 <.1 10 1.9 200 0 20 72 .2 17 1.1 40 320 57 24 29 42 .6 370 18 39 34 38 .4

2.7 17 36 <.1 13 II 100 22 4040 Ca-HC03 1.6 16 27 .3 32 .66 6 14 4040 Ca-HC03 1.0 8.0 33 .1 17 .98 5

1.3 9.2 30 .1 II .96 8 4 4040 Ca-HC03 .9 7.7 6.2 .1 7.2 .27 5

1.0 240 0 6.9 14 <.1 17 2.0 10 100 1.8 25 75 .2 II 1.10 10 2 4040 Ca-Mg-Na-HC03 2.0 II 5.5 .1 19 .13 240 20 4040 Ca-HC03 1.1 15 3.9 <.1 6.5 .32 210 19 4040 Ca-HC03 .9 7.4 II <.1 13 .27 110 4 4040 Ca-Mg-Na-HC03

.6 II 4.5 <.I II .99 21 3 4040 Ca-HC03 .6 8.4 7.7 <.1 9.1 .47 5 12 4040 Ca-HC03 .4 9.9 7.3 <.1 11 1.70 4 <1 4040 Ca-HC03 1.9 6.3 12 .2 24 .31 18 26 4040 Ca-HC03 5.2 18 6.5 .7 49 .11 33 7 4040 Ca-Na-HC03 .7 16 8.4 .1 17 .41 17 3 4040 Ca-Mg-HC03 1.5 8.6 10 .1 12 .97 4 8 4040 Ca-HC03

55 Table 9. Chemical analyses of water samples from springs

[ft3/s, cubic feet per second; "C, degrees Celsius; IlSlcm, microsiemens per centimeter at 25 degrees Celsius; mg/L, milligrams per liter; Ilg/L, micrograms Location: See figure 2 for description of data-site numbering system. Sampling method codes: 70, dip sample.

Flow Spe- Hard- Alka- Solids, rate, cific Hard- ness, Iinity, sum of Date instan- conduct- pH Temper- ness noncar- lab constituents, of taneous ance (stand- ature (mglL bonate (mglL dis- Location Sample (tt3/s) (IlS/cm) ard (DC) as (mgIL as solved units) CaC03) CaC03) CaC03) (mglL)

(A-6-2)27dcc-S I 09-17-85 1.6 430 7.5 9.5 220 17 207 240 (A-7-1)19dbc-S I 09-11-85 .25 280 7.8 10.0 140 21 123 160 (A-7-1)22caa-SI 01-24-85 175 7.2 24.0 58 0 61 100 (A-7-1)30aca-SI 09-11-85 350 8.0 7.0 190 21 173 200 (A-7-3)23acb-S I 09-17-85 '20 390 8.2 6.5 220 17 201 220

Seepage from unconfined aquifer southwest of Huntsville 10-31-85 1. 04 445 7.7 12.0 260 10 246 280 Seepage from unconfined aquifer northwest of Huntsville 10-31-85 .01 450 8.4 12.0 250 23 232 270

1Estimated value.

budget that the application rate is the same for all irri­ evaporation from canals orditches, part runs out the tail gation techniques. This rate is estimated to be 1 acre­ end of the ditches into Pineview Reservoir, part infil­ foot per acre per month. The rate is based on specifica­ trates the soil and recharges the aquifer directly beneath tions given for the Causey project, which provided irri­ the canals or ditches, and the remainder infiltrates the gation water from Causey Reservoir (N.W. Plummer, soil beneath irrigated acreage and recharges the valley­ Regional Director, U.S. Bureau of Reclamation, oral fill aquifer system. commun., 1981). The total delivery rate necessary for For this study, it was assumed that 5 percent of an application rate of I acre-foot per acre per month on the delivered water was lost to evaporation and 10 per­ the early-season irrigation acreage is 118 cubic feet per second. The desired delivery rate from August through cent ultimately flowed into Pineview Reservoir and out of Ogden Valley. Crop consumptive use in Ogden Val­ September decreased to 107 cubic feet per second. ley was determined by G.B. Pyper (U.S. Geological The delivery rate from May through July 1985 Survey, oral commun., 1986) with a method that was fully met by surface-water flows. The desired accounted for crop type and acreage, daylight hours, air delivery rate from August through September was not temperature, and precipitation. met by surface-water flows during that entire period, Seepage to the aquifer from irrigation canals but the consumptive-use needs of the crops were (irrigation distribution losses) is small and varies assumed to be fully satisfied. The monthly delivery rate throughout the irrigation season. Some canals did not for 1985 was estimated as the greater of either the receive water throughout the season; other canals con­ desired delivery rate for the acreage irrigated or the tinued to receive water after the irrigation season was average monthly surface-water flow into Ogden Valley, over. Water from the Mountain Valley (or Ogden Val­ as determined from a proportion of the South Fork Ogden River streamflow. ley) Canal did not flow past the Middle Fork Ogden River until sometime in June; in the summer, the mea­ Not all of the water diverted for irrigation is lost sured net loss was 4.0 cubic feet per second (Herbert to crop-consumptive use. Part of the water is lost to and others, 1987). The West Ditch lost 0.8 cubic feet

56 per liter; <, constituent concentration less than indicated detectable limit]

Nitro- Methy- Magne- Potas- Chlo- Fluo- gen, Manga- lene Calcium, slum, Sodium, sium, Sulfate, ride, ride, Silica, N02 +N03, Iron, nese, blue Sam- dis- dis- dis- dis- dis- dis- dis- dis- dis- dis- dis- active piing solved solved solved solved solved solved solved solved solved solved solved sub- method, (mgfL (mgfL (mg/L (mg/L (mg/L (mg/L (mg/L (mg/L as (mg/L (~gfL (~gfL stance codes as Ca) as Mg) as Na) as K) as 504) as CI) as F) 5i02) as N) as Fe) as Mn) (mgfL)

60 18 7.7 1.3 8.9 9.4 <0.1 10 0.65 <3

76 16 7.0 5.4 1.0 6.1 .2 12 .54 .03 70

74 17 7.4 3.9 9.8 8.2 .1 11 .26 .03 70

per second, but was dry after the first of August. The water recharging the aquifer was determined for each upper Eden Canal lost 1.2 cubic feet per second, and month of irrigation in 1985 as follows: Wolf Creek Ditch lost 0.4 cubic feet per second. The Huntsville South Bench Canal and the Eden Canal Month DR L CCR IR diverted water for livestock until sometime in Novem­ May 118 -(0.15)(118) -12.5 = 87.8 (75 percent) ber. Other canals and ditches showed minor losses. June 118 -(0.15)(118) -40.7 =59.6 (50 percent) The quantity of irrigation water recharging the July 118 -(0.15)(118) -65.5 = 34.8 (30 percent) August aquifer in 1985 was estimated with the following equa­ 101 -(0.15)(101) -46.6 =39.3 (40 percent) September 79 -(0.15)(79) - 8.9 = 58.3 (75 percent) tion: IR = DR -L -CCR (1) where IR = the quantity of irrigation water Losing Streams recharging the aquifer, in cubic feet Miscellaneous measurements made in February per second; and March 1985 (table 4) can be used to identify DR = the quantity of delivered water, in reaches where recharge takes place and the quantity of cubic feet per second; flow that recharges the aquifer system from streams L = loss of delivered water, in cubic feet during the winter months. In the first reach ofthe North per second, by evaporation and canal Fork Ogden River, about 2.4 cubic feet per second flow into Pineview Reservoir; and seeped to the aquifer; in the second reach of the North Fork Ogden River, about 7.6 cubic feet per second CCR crop consumptive use, in cubic feet = seeped to the aquifer. Although the last measured reach per second. ofNorth Fork Ogden River indicates a net gain from the The quantity of irrigation water recharging the aquifer, it was estimated that the upper part ofthis reach aquifer and the approximate percentage of delivered actually loses about 2 cubic feet per second to the aqui-

57 Table 10. Water budget for the valley-fill aquifer system, mid-February 1985 through January 1986

[Values are in cubic feet per second]

Winter Mid-February Mid·March Mid-April May 1985 to mid-March to mid-April to May (period 1) (period 2) (period 3) (period 4)

Estimated recharge

Precipitation 0 9 120 0 0 Irrigation 0 0 0 0 88 Irrigation distribution losses 0 0 0 0 6 Losing streams 67 69 140 140 105 Subsurface inflow 48 48 48 48 72 Total 115 126 308 188 271

Estimated discharge

Gaining streams 48 48 93 93 93 Springs and drains 22 27 32 29 51 Ogden well field 15.0 14.4 15.4 18.4 13.9 Other wells .1 .1 .1 .1 .3 Evapotranspiration 0 0 0 1 13 Pineview Reservoir 45 45 60 78 88 Total 130.1 134.5 200.5 219.5 259.2

fer. In the measured reach of the Middle Fork Ogden Estimated recharge from minor perennial streams during late River, about 4.3 cubic feet per second seeped to the winter 1985 aquifer. Recharge from the South Fork Ogden River was estimated at 46 cubic feet per second (Browning, Stream Recharge (cubic feet 1925, p. 17-20). per second)

Starting in May, diversions from streams into Bally Watts Creek 0.5 canals decreased water depths in the stream channels; Maple-Kelley Canyon creek .7 the estimated recharge to the aquifer system was 25 per­ WolfCreek 1.0 cent less than the pre-diversion value. The North Fork Pole Canyon Creek .5 Sheep Creek 1.0 Ogden River above the first diversion structure was Cold Canyon Creek .5 estimated to lose 4 cubic feet per second to the aquifer, Cobble Creek .5 but the flow was entirely diverted at the first diversion Geertsen Canyon creek .5 structure. Flow in the Middle Fork Ogden River was entirely diverted in June. Flow in the South Fork Spring snowmelt on the hillsides surrounding Ogden River exceeded the capacity of the diversion Ogden Valley was assumed to temporarily increase structure in June, and water flowed down the entire flow in the minor perennial streams. Some channels reach ofthe stream channel. It was estimated that about that were dry all winter also had flow during the snow­ 46 cubic feet per second from the South Fork Ogden melt period. Spring snowmelt increases the potential River recharged the aquifer during June 1985. for increased recharge during the early spring. It was estimated that recharge from flow in minor perennial Estimated recharge from the remaining perennial streams doubled during the snowmelt period. Starting streams during the winter months is as follows: in June, all minor streams except Geertsen Canyon

58 June July August September October November December January

(period 5) (period 6) (period 7) (period 8) (period 9) (period 10) (period 11) (period 12)

Estimated recharge 0 0 0 0 34 80 10 0 60 35 39 58 0 0 0 0 6 6 5 5 2 2 0 0 51 16 16 16 39 75 67 67 96 154 91 72 48 48 48 48 213 211 151 151 123 205 125 115 Estimated discharge 103 73 45 42 33 41 89 48 50 34 22 21 14 25 18 32 14.1 14.6 15.1 10.1 9.3 13.6 13.0 12.7 .3 .3 .3 .3 .1 .1 .1 .1 44 71 50 10 3 0 0 0 88 78 78 60 60 60 60 78 299.4 270.9 210.4 143.4 119.4 139.7 180.1 170.8

creek and Wolf Creek were entirely diverted at the val­ ond recharged the aquifer in that reach. In November, ley margin for irrigation. conditions generally were back to those ofthe previous From July through September, all streams except winter. for short reaches above the upper diversion structures on the North Fork Ogden River and the South Fork Pineview Reservoir Ogden River were entirely diverted or otherwise dry at It was initially assumed for the preparation ofthe the valley margin. It was estimated that 2 cubic feet per water budget that seepage downward from Pineview second recharged the aquifer system above the upper Reservoir into the principal aquifer did not occur. If diversion structure on the North Fork Ogden River, and downward seepage does occur, it would be the water 14 cubic feet per second recharged the aquifer above induced from Pineview Reservoir by pumpage from the the diversion structure on the South Fork Ogden River. Ogden well field; the amount of seepage could not be In October, the diversions generally were greater than the amount of pumpage. stopped, and flow was restored. Minor perennial streams again flowed in their channels and recharged Subsurface Inflow the aquifer at their previously estimated rates for Feb­ ruary. Water still was partially diverted at the upper Much of Ogden Valley is underlain by the Nor­ North Fork Ogden River and the South Fork Ogden wood Tuff, which is not permeable in most areas. In a River diversion structures. It was estimated that 7 cubic few areas, either Paleozoic carbonate rocks or the feet per second passed the diversion structure on the Wasatch Formation probably underlie the valley-fill North Fork Ogden River, and subsequently recharged deposits, facilitating ground-water inflow from the bed­ the aquifer system. On the South Fork Ogden River, rock. where water also passed the diversion structure, a small Little information is available to derive the amount offlow was observed at the first county bridge. inflow from bedrock to the valley-fill deposits. The Browning (1925) indicated that 24 cubic feet per sec- Darcy equation was used to estimate the inflow during

59 stable conditions for the winter when snowmelt was not Discharge occurring. It was assumed that all inflow from the bed­ rock occurred along the vaHey perimeter, which is The valley-fill aquifer system loses water about 208,000 feet long. The hydraulic conductivity of because ofvarious types ofdischarge. Each type ofdis­ the bedrock was estimated to be I foot per day. When charge was analyzed separately to provide detailed infiltration of snowmelt was not occurring, the average analysis of the ground-water-flow system. hydraulic gradient was estimated to be 0.2 foot per day, and the average saturated thickness ofthe bedrock-flow Gaining Streams system contributing to the valley-fill deposits was 100 feet. Using the Darcy equation, Miscellaneous measurements made in February 1985 (table 4) indicate discharge from the valley-fill Q=KIA aquifer system to a number of stream channels. Many where Q = discharge, ofthe gaining reaches are located in the southern part of Ogden Valley. The reach of the North Fork Ogden K = hydraulic conductivity, River above site NIl gained about 7.3 cubic feet per I = hydraulic gradient, and second. The next downstream reach on the North Fork A = cross-sectional area through which Ogden River gained 3.9 cubic feet per second after flow occurs; accounting for a possible loss of2 cubic feet per second subsurface inflow when snowmelt was not contributing in the upper part of the reach. Bennett Creek showed a to the ground-water system was about 48 cubic feet per gain of about 5.1 cubic feet per second. second. The remaining gaining reaches are along the Subsurface inflow from the bedrock to Ogden major stream channels upstream from Pineview Reser­ Valley increases dramatically because of snowmelt voir. From existing gaging station records, it was esti­ infiltration in the area surrounding the valley. Burnett mated that the North Fork Ogden River gained 6 cubic Spring [(A-7-1)22dad-SI], which supplies Eden with feet per second in the unmeasured reach just above much ofits municipal water, discharges from the valley Pineview Reservoir, the Middle Fork Ogden River fill, but the actual source of the water is thought to be gained an estimated 4.5 cubic feet per second, Geertsen the underlying bedrock of Norwood Tuff or metasedi­ Canyon creek gained an estimated 1.5 cubic feet per mentary rocks. The average rate ofspring flow in 1985, second, and the South Fork Ogden River gained an esti­ before snowmelt occurred, was 48 gallons per minute mated 19 cubic feet per second. These gains were (National Water Use Data System, Division of Water assumed constant from February through mid-March. Rights, Utah Department ofNatural Resources, written From mid-March through May, it was assumed commun., 1986). For May through September, the that discharge from the valley-fill aquifer system to the average monthly rate of spring flow was as follows: downstream reaches of the streams increased. Dis­ Average monthly rate of flow of Burnett Spring charge to all the streams, except Bennett Creek, was [(A-7-1)22dad-S1] for May through September 1985 estimated to have doubled compared to the discharge during winter conditions. Bennett Creek mostly drains Average monthly rate water from the Wasatch Formation during mid-March of spring flow through May, and flow is steady. Month (gallons per minute) Discharge from the aquifer system to the streams May 71 decreases from June through October as shown in table June 98 10. Declining water levels in wells in the southern part July 154 of the valley also indicate that discharge from the aqui­ August 89 fers is declining. Flow in the North Fork Ogden River September 74 downstream from the springs is estimated to have decreased by 5 cubic feet per second. Flow in Bennett Creek doubled from seepage of irrigation water applied The variability in subsurface inflow from the bedrock over much ofits drainage in the valley. Discharge from (table 10) was estimated from the changes in flow of the aquifer system to Geertsen Canyon creek is Burnett Spring. assumed to remain fairly constant.

60 From August to November, discharge to streams of increased natural recharge in the spring and reduced was reduced further. Discharge to the lower reach of ground-water discharge to the reservoir because of the the North Fork Ogden River is estimated to have increased stage of the reservoir. The water-level rise decreased another 5 cubic feet per second. Flow in suggests that additional pumpage from the Ogden City Bennett Creek decreased to about 5 cubic feet per sec­ well field is feasible because an increase in natural ond after seepage of irrigation water ceased. Discharge recharge and in the stage of Pineview Reservoir have a to Geertsen Canyon creek remained fairly constant as greater effect on water levels than an increase in pump­ estimated during this study. age. In December, increases in flow recorded at the Total pumpage from other wells was small when gaging stations were estimated to equal gains made by compared to pumpage from the Ogden well field (table the streams in the southern part ofthe valley. Discharge 10). Pumpage from wells in the smaller public systems to Bennett Creek and Geertsen Canyon creek stayed was obtained from the National Water-Use Data Sys­ fairly constant from the previous period. tem (Division of Water Rights, Utah Department of Natural Resources, written commun., 1986). Pumpage Springs and Drains from the unmeasured community systems was esti­ mated on a per-user basis. Pumpage from each of the Springs and drains in Ogden Valley consist of remaining wells, which are used for domestic purposes perennial springs and spring-fed reaches of stream or stock watering, was estimated as I acre-foot per year. channels including Liberty Springs, Liberty Spring Very few wells are used exclusively for stock watering Creek, Bailey Spring, Spring Creek, small seeps that (table 7). Half of the annual total water pumped from emerge in the draws near the edge of the confining these wells was assumed to be used during May layer, and seeps that occur in the area periodically inun­ through September because ofthe increase in lawn and dated by Pineview Reservoir. garden watering. Measurements made in February 1985 (table 4) and estimates of the reservoir seeps give a total dis­ Evapotranspiration charge from springs and drains of about 22 cubic feet per second. The total discharge by springs and drains About 11,500 acre-feet of water is consumed for Ogden Valley during each water-budget period was annually by natural vegetation and subirrigated crop­ determined by the proportion that Spring Creek dif­ land. In order to adjust this annual rate for the monthly fered from its base-flow rate during the winter (table conditions that occurred in 1985, the proportional rates 10). ofmonthly crop consumption were determined by G.E. Pyper (U.S. Geological Survey, written commun., Wells 1986). The monthly proportion of annual evapotrans­ piration, the monthly evapotranspiration, and the The average monthly pumpage rate ofthe Ogden evapotranspiration rates determined by monthly crop well field fluctuated during 1985 as shown in table 10. consumption for 1985' and adjusted for variable cli­ The fluctuation for a 5-day interval is shown in figure matic conditions are as follows: 22. Pumpage is erratic but generally increases in the Monthly proportion of annual evapotranspiration, monthly spring when water demand increases in Ogden. The evapotranspiration, and evapotranspiration rates for 1985 pumpage stabilizes when the filtration plant opens for the summer and starts treating water diverted from Monthly Monthly Evapo­ Pineview Reservoir. Pumpage decreases in the fall proportion evapo- transpiration when water demand begins to decline. The filtration of annual transpiration rate Month evapotranspiration (acre-feet) (cubic feet plant usually continues to treat reservoir water until late per second) October. Hydrographs for water-level altitudes in a well Late April 0.005 58 1.0 May .07 805 13.5 completed in the confined part of the principal aquifer June .23 2,645 44.4 near the Pineview Reservoir and for the stage ofPinev­ July .37 4,255 71.5 iew Reservoir are shown in figure 22. The water level August .26 2,990 50.2 September .05 575 9.7 in the well rose during increased pumpage from the October .015 172 2.9 Ogden well field. The rise resulted from a combination Total 1.000 11,500 193.2

61 300 ....J- ~ a:: QUANTITY OF WATER PUMPED W 250 FROM OGDEN WELL FIELD I-z ~ 0, L[) 200 a:: I- OW UJ u. u. Ww <9 a:: 150 a:: U I«« U~ (J) 100 0 U a:: I- W :::2: 50 ::J ....J 0 > 0 J A S 0 NDJ FMAM JJ A SON DJ F MAM JJ 1984 I 1985 I 1986 4,920

WELL (A-6-2)18BAD-1

....J W 4,910 ~ >UJ ....J « UJ (J) UJ > 0 4,900 «co I- W W u. z 4,890 ..i W > W ....J a:: W ~ 4,880 ~ / STAGE OF PINEVIEW RESERVOIR

4,870 L...-..L.-..l.---'------'------'------'-----'----I.-----''-----J...--..L.-..l.---'------'------'------'-----'----I.-----''--'---'-----'------'------'------'-----'----J J ASOND J FMAMJ J ASONDJ FMAMJ J 1984 I 1985 I 1986 Figure 22. Ogden well-field pumpage, water level in well (A-6-2)18bad-1, and stage of Pineview Reservoir, July 1984 through July 1986.

62 Pineview Reservoir the Wasatch Formation where the Norwood Tuff is absent. It also is possible that water drains into perme­ Upward seepage through the lakebed was mea­ able bedrock 3.5 miles west of Liberty and 5 miles sured in July 1986 when the stage of Pineview Reser­ south of Huntsville. Because ofthe lack ofevidence·of voir was slightly below its maximum of 4,900 feet. A any outflow, it was presumed to be negligible. seepage-measurement site was located in each of the "arms" ofPineview Reservoir (pI. 2). The total amount of seepage was estimated by integrating the seepage SIMULATION OF GROUND-WATER FLOW rates at the measurement sites over the entire reservoir IN THE VALLEY-FILL AQUIFER SYSTEM area. The total amount of seepage to Pineview Reser­ voir from the principal aquifer at the time of the seep­ A finite-difference, three-dimensional computer age measurements was estimated to be 86.7 cubic feet model was used to simulate ground-water flow in the per second. valley-fill aquifer system of Ogden Valley. The com­ puter program used was developed by McDonald and Estimated seepage to Pineview Reservoir, July 1986 Harbaugh (1984). Most ofthe data used for calibration of the steady-state and transient model simulations are Reservoir Upward seepage arm (cubic feet per second) presented in previous sections of this report. The computer-model simulation was done in North Fork Ogden River 16.5 order to improve understanding ofthe hydrology ofthe Middle Fork Ogden River 35.0 South Fork Ogden River 19.2 valley-fill aquifer system, including the areal distribu­ Lower area (southwestern part of reservoir 16.0 tion and range in values of the hydraulic properties. exclusive of the three arms) Few data on the subsurface geology have been col­ Total 86.7 lected and analyzed other than data for the now-aban­ doned Ogden artesian well field and vicinity. Adjustments to the initial hydraulic-property values of The quantity of seepage during the winter was the aquifer system during calibration were made on the estimated using the same seepage rates for a smaller basis of flow rates to and from streams and Pineview area of the reservoir. The quantity of seepage to Pinev­ Reservoir and the agreement between measured and iew Reservoir during the winter was estimated to be computed ground-water levels. 45.5 cubic feet per second. Estimated seepage to Pineview Reservoir during winter Two hypothetical changes to the water budget were simlflated to observe the resulting effects on Reservoir Upward seepage streamflow and ground-water levels. A I-year drought arm (cubic feet per second) and withdrawals from three additional wells were sim­ ulated to estimate the magnitude and distribution ofthe North Fork Ogden River 9.0 effects from such conditions. Middle Fork Ogden River 14.0 South Fork Ogden River 14.4 Lower area (southwestern part of reservoir 8.0 Model Design and Assumptions exclusive of the three arms) Total 45.4 The valley-fill aquifer system in Ogden Valley was simulated using two layers (fig. 23). The upper The quantity of seepage for spring and fall reser­ layer, layer I, represented the shallow water-table aqui­ voir levels of 4,876; 4,880; 4,890; and 4,900 feet was fer and was active only in the southern part ofthe valley estimated by integrating seepage rates over the area of above the confining layer. Layer I was not simulated in the reservoir. The quantity of possible downward seep­ the area perennially inundated by Pineview Reservoir age was not subtracted from these estimates (table to). because the bottom of the reservoir is incised into the confining layer. The lower layer, layer 2, represented Subsurface Outflow the principal aquifer and was active throughout the sim­ ulated area. Layer 2 was simulated with an option in Outflow from the valley-fill aquifer system to the the computer model (McDonald and Harbaugh, 1984, bedrock surrounding Ogden Valley is unlikely. It is p. 151) that allows the use of either the storage-coeffi­ possible that water drains into the carbonate rocks or cient value or specific-yield value. If the water level is

63 ~

Southwest ---Northeast ..- Ground-water flow direction

CONSTANT Q) u FLUX ~~ INFLOW :::J~ l/) ·5 Uo­ "i:: etS Q>-o OUT E Q) .2.§ Springs, drains, stream -c c0 gains, wells, and ~ u evapotranspiration ~o

a n c e ~ ~ ~~ LAYER 2 (Principal aquifer) I

OUTFLOWFLUX ~ ....- NO" F,gl{1l"%"'"" ""

Figure 23. Schematic section of the two-layer ground-water flow model simulating the aquifer system in Ogden Valley. above the top of layer 2, the storage-coefficient value is The general-head-boundary feature of the model used. If the water level is below the top of layer 2, the (McDonald and Harbaugh, 1984, p. 343-369) was used specific-yield value is used. Flow between layer 1 and to simulate variable leakage between the confined part layer 2 through the confining layer was simulated using of the principal aquifer and Pineview Reservoir. Gen­ values of vertical hydraulic conductivity of the confin­ eral-head-boundary cells were specified in layer 2 to ing layer divided by the average thickness ofthe confin­ delineate the area inundated by Pineview Reservoir ing layer (vertical conductance) (McDonald and during each stress period. General-head-boundary cells Harbaugh, 1984, p. 151). In this case, vertical conduc­ were added or removed during successive stress peri­ tance of the aquifer material does not slow vertical ods as the area inundated by Pineview Reservoir ground-water movement, compared to the confining expanded or contracted. Layer I was kept active in the layer, and thus, can be ignored. area not perennially inundated by Pineview Reservoir, but it did not account for much storage in the aquifer. A block-centered grid with variable spacing was used to divide a map of the valley-fill aquifer system The top boundary of the model was the water­ into discrete cells (fig. 24). The grid spacing was table surface in layer I, or layer 2 where layer 1 was smaller on the west side of the model grid to allow absent; and the bottom boundary was a no-flow bound­ accurate location of hydrologic boundaries and ary (fig. 23) representing the Norwood Tuff in most of stresses. The grid consists of 59 rows and 23 columns. the valley underlying layer 2. Water-table conditions The rows are spaced 1,340 feet apart. The columns are existed throughout layer 1 and in layer 2 where layer I spaced from 1,320 to 1,340 feet apart on the west side was not simulated, except in the area that was perenni­ ofthe grid and from 1,540 to 1,640 feet apart on the east ally inundated by Pineview Reservoir. In the part ofthe side ofthe grid. Ofthe 1,357 total cells in each layer in model where layer 1 was active, flow between the two the grid, 782 cells in layer 2 are active and 139 cells in layers was controlled by a verticalleakance value that layer 1 are active. simulated the hydraulic characteristics of the confining layer.

Model Boundary Conditions Streams The entire model area was surrounded by con­ The North Fork Ogden River, Middle Fork stant-flux cells. The active cells at the periphery of the Ogden River, and South Fork Ogden River were simu­ model represented consolidated rock and valley fill that lated by river cells. Because ofthe substantial changes is mainly slopewash with a relatively small hydraulic that occur in flow ofstreams in Ogden Valley, the stage conductivity along the edge of the valley. Recharge at height and distribution of active streams sometimes most ofthe periphery cells simulated subsurface inflow change abruptly. Data used in the simulation to from the bedrock to layer 2, the principal aquifer. describe these changes were based on field observa­ Subsurface inflow was estimated to be generally tions of streams throughout the valley. small. It is larger where the valley fill is underlain by In their upper reaches, an unsaturated zone sepa­ permeable carbonate rock or faults that transmit water rated many streams from the unconfined part of the in consolidated rock. principal aquifer. When the streambed was above the Initially, the simulated subsurface inflow was 48 water level in the aquifer, simulated leakage from the cubic feet per second distributed uniformly to the con­ river cell was directly proportional to the streambed conductance (McDonald and Harbaugh, 1984, p. 214). stant-flux cells. The inflow was kept relatively constant but was redistributed until simulated water levels were The use ofriver cells enabled a precise quantity of leak­ similar to measured water levels in the aquifers. The age to be allowed from those river cells, and leakage hydraulic conductivity of the cells at the periphery, was used as a calibration tool to adjust simulated water which represent the thin valley fill and underlying con­ levels. The quantity of leakage was not varied if it had solidated rock, generally was kept to a value that pro­ been determined either by seepage runs made in Febru­ duced a transmissivity of less than 200 feet squared per ary 1985 or by analysis of other previously collected data. day. The two constant-flux cells located at Pineview Reservoir simulated discharge from the ground-water­ Canals and ditches that were not surrounded by flow system to the south end of Pineview Reservoir. irrigated fields also were simulated by river cells.

65 EXPlANATION

Active cell in layers 1 and 2

Active cell in layer 2, 111"52'30' LJ inactive cell in layer 1 I Active cell in layer 2, inactive cell in layer 1 Pineview Reservoir

• Inactive cell in layers 1 and 2

W Model boundary steady-state recharge - Approximate recharge rate, in cubic feet per second, multiplied by 10-1

(-) Model boundary steady-state discharge

• Node representing observation well

R.1W. R.1 E.

41"15'-

Base from U.S. Geological Survey Ogden, 1: 100,000, 1976

o 2 3 MILES I I I I o 2 3 KILOMETERS R.1 E.

Figure 24. Model grid, areal distribution of active cells, and boundary steady-state recharge and discharge for the model of the ground-water system in Ogden Valley.

66 Recharge from canals and ditches was considered min­ transpiration rate of 3 feet per year was determined by imal when compared to recharge from irrigated fields. G.E. Pyper (U.S. Geological Survey, written commun., 1986). The model program also adjusted the evapo­ Drains transpiration rate according to the depth of the water table below land surface. The rate was reduced by a Drain cells were used in the model to simulate straight-line proportion to an extinction depth of the outflow from the aquifer to drains, but they did not water table, which was specified as 30 feet below land allow flow from drains to the aquifer. Thus, the drain surface. cells also can be used to simulate streams that are perennially gaining as well as simulating irrigation Areal Recharge drains. Liberty Spring Creek and most ofSpring Creek were simulated by drain cells. Most ofthe flow ofthese Recharge from precipitation was assumed to creeks originates from ground-water discharge within occur in March and April from infiltration of snowmelt Ogden Valley. Drain cells also were used to simulate and from October into December before the first lasting irrigation drains and small seeps that were near Pinev­ snowpack. A total of 33 percent of the precipitation iew Reservoir in the low-lying areas, when the seeps during each period was recharged to the ground-water­ were not inundated by the reservoir. The lower reaches flow system. All precipitation bound up in snow accu­ of some irrigation ditches probably drain some ground mulation from December into March was recharged water during the irrigation season; however, the during March and April. Precipitation was distributed affected reaches were not identified, and this drainage throughout the valley as shown by the U.S. Weather was not incorporated into the model. Bureau (1963) map of average annual distribution. Recharge from irrigated fields was determined by Wells several factors. The mapped irrigated acreage was used Nearly all of the ground water pumped in Ogden to determine the proportional area of irrigated fields to Valley is from the Ogden well field located on the the total area that would be in each model cell. The rate southern tip of the promontory between the North Fork of water recharging the ground-water-flow system was Ogden River and the Middle Fork Ogden River arms of determined by the delivery rate of surface water minus Pineview Reservoir. The measured discharge for each the losses by evaporation, canals, and crop-consump­ of the periods simulated by the model was used as the tive use. These two factors were combined to deter­ rate for that water-budget period (table 10). mine an adjusted recharge rate from irrigated fields during each period. The recharge rate varied from 30 to Discharge from wells for the three known com­ 75 percent of the available surface-water supply. munity systems and all other known domestic and stock wells also was simulated, although the total withdrawal Recharge from septic systems occurs throughout was minimal compared to the withdrawal from the the valley. The only substantial recharge from septic Ogden well field. Withdrawals by the Nordic Valley systems is at Huntsville. An average recharge rate of system were measured; withdrawals by the Eden Hills 0.2 cubic foot per second from septic systems was and Lakeview systems, in addition to the domestic and divided among seven cells representing the Huntsville area. stock wells, were estimated by per capita and seasonal use. All other community water systems and individual users obtain their water from sources other than wells in Hydraulic Properties the valley-fill aquifer system, and their use was not The ground-water-flow system in Ogden Valley incorporated into the model. is controlled partly by the hydraulic characteristics of the aquifers. The estimated values ofthese characteris­ Evapotranspiration tics were included in the model data and adjusted dur­ ing model calibration. Evapotranspiration was simulated throughout the uppermost active model layer, although the rate was Hydraulic conductivity adjusted for several factors. The maximum possible evapotranspiration rate was adjusted for the propor­ A uniform hydraulic-conductivity value, the tional density ofmapped phreatophytes in each cell and value determined from the aquifer test of the Ogden the proportional monthly consumptive use. An evapo- well field, was used initially for most ofthe cells in the

67 computer model. Modifications of the hydraulic-con­ Storage coefficient ductivity distribution were made during calibration. A constant storage-coefficient value of 1 x 10-4 Hydraulic-conductivity values were adjusted concur­ was used during the calibration process for the areas rently with changes in the boundary recharge until the where the principal aquifer was confined. A constant calculated transmissivity values of the cells at the specific-yield value of 0.10 was used for the areas periphery, which represent a veneer of slope-wash where water-table conditions prevailed. deposits and bedrock comprised of either Norwood Tuff or carbonate rocks, were less than 200 feet squared Vertical hydraulic conductivity per day. Vertical hydraulic-conductivity values are a mea­ Hydraulic-conductivity values were changed to sure of the ability of ground water to flow in a vertical adjust the rate that stresses were propagated through the direction. The principal aquifer was separated from the system in order to generally match water-level altitudes shallow water-table aquifer by a leaky confining layer, at observation wells during steady-state simulation and and a vertical hydraulic-conductivity value was to match water-level changes during the transient sim­ assigned to each active cell in layer 1 to control the ulation. The resulting hydraulic-conductivity values exchange of water between layer I and layer 2. for layer 2 ranged from less than 1 foot per day in the Data obtained from reservoir-bed seepage exper­ areas around the margin ofthe valley to slightly greater iments enabled a vertical hydraulic-conductivity value than 300 feet per day in the area east of Huntsville (fig. to be estimated for each of three seepage-measurement 25). The range of hydraulic-conductivity values for sites (pI. 2). Because the values differed slightly at each layer 1 was less than 10 to 50 feet per day (fig. 26). The of the sites, different values of vertical hydraulic con­ model simulation was relatively sensitive to different ductivity were used for the three arms ofPineview Res­ hydraulic-conductivity distributions, particularly near ervoir. The vertical hydraulic-conductivity values used recharge or discharge areas. for the transient simulation were 0.04 foot per day in the North Fork Ogden River arm, 0.03 foot per day in The hydraulic-conductivity values and the satu­ the Middle Fork Ogden River arm, and 0.01 foot per rated thickness were used to calculate transmissivity day in the South Fork Ogden River arm. These values values for the principal aquifer. On the basis ofdrillers' are about three to four orders ofmagnitude less than the logs and a surface-water resistivity survey, the saturated horizontal hydraulic-conductivity values of the princi­ thickness of layer 1 (shallow unconfined aquifer) was pal aquifer in the area. Each vertical conductivity value generally less than 90 feet. Saturated thickness oflayer was divided by 70 ft [the average thickness of the con­ 2 (principal aquifer) ranged from about 100 feet near fining layer according to Thomas (1945)] to determine the valley margins to about 700 feet in the area east of the model value "VCONT" (McDonald and Harbaugh, Huntsville. Saturated thickness and hydraulic-conduc­ 1984, p. 151), which allows for the simulation of verti­ tivity values used in the model were initially extrapo­ calleakance of water through a confining layer. lated from only a few data points. During model Model simulation was fairly sensitive to differ­ calibration, these values were adjusted, within reason­ ences in vertical hydraulic conductivity. A decrease in able limits, to allow simulated heads to more closely vertical hydraulic-conductivity values caused an match measured water levels. Transmissivity values increase in hydraulic head in layer 2, an increase in dis­ ranged from 20 to 230,000 feet squared per day. The charge to the river and drain reaches just upstream from largest transmissivity values were assigned to the area Pineview Reservoir, and a decrease in discharge from north of the South Fork Ogden River channel east of layer 2 to the reservoir. Huntsville. Other areas of relatively large transmissiv­ ity values were beneath Pineview Reservoir and near Initial Conditions Liberty. The transmissivity values in the main valley Actual pre-development steady-state conditions and near Liberty typically were equal to or greater than are unknown. For the purposes ofthis investigation and 50,000 feet squared per day; however, the transmissiv­ computer simulation, it was assumed that the ground­ ity values in the area near Eden that separates the Lib­ water-flow system was in a steady-state condition dur­ erty area from the main valley typically were less than ing the low-flow period in mid- to late-February 1985. 500 feet squared per day. The water levels in the principal aquifer, the stage of

68 EXPlANATION Hydraulic conductivity, in feet per day

Ot05 111 0 52'30" c=J I 11 Mlil! ,~ 5 to 50

• 50 to 100

fiftfjH 100 to 200

• Greater than 200

D Inactive cell

R.1W.

Base from U.S. Geological Survey \ Ogden, 1:100,000. 1976

o 2 3 MILES I I I I I o 2 3 KILOMETERS R.1 E.

Figure 25. Distribution of hydraulic-conductivity values for layer 2 (principal aquifer) of computer model for Ogden Valley.

69 EXPLANATION Hydraulic conductivity, in feet per day

oto 10 111"52'30" I 10 to 15

'".:: .. •EfJ!JJ:::::::: 15 to 30 ~ 30 to 50 CJ Inactive cell

R.1W.

Base from U.S. Geological Survey Ogden, 1:100,000, 1976

2 3 MILES I °I I I ° 2 3 KILOMETERS R.1 E.

Figure 26. Distribution of hydraulic-conductivity values for layer 1 (shallow water-table aquifer) of computer model for Ogden Valley.

70 Pineview Reservoir, and the pumpage from the Ogden model data. Next, flow rates to and from the major well field had been fairly steady for about a month (fig. stream channels were adjusted by iteratively adjusting 22). The surface-water inflow to Ogden Valley also the streambed conductance values (McDonald and Har­ was steady during February 1985 (fig. 9). Flow in the baugh, 1984, p. 209-217) and the hydraulic conductiv­ South Fork Ogden River remained fairly stable for ity of the underlying aquifer. Last, the water-level about a month, although flow during February was sub­ altitudes in observation wells were simulated to match stantially greater than that earlier in the winter. measured water-level altitudes to within one-half ofthe Wheeler Creek, a smaller, unregulated watershed, contour interval from the 7.5-minute topographic maps showed very little change in flow during the same ofthe area near the well. These calibration criteria were period. flexible in areas that had relatively large hydraulic gra­ This assumption of steady state may introduce dients. some error into the simulated water-level changes for A steady-state calibration was obtained; but, dur­ 1985-86. The steady-state assumption was checked by ing transient calibration, minor changes in hydraulic running the transient-state model simulating uniform conductivity were made that caused changes in water February 1985 conditions for a 12-month period. This levels or in discharge. The steady-state simulation was simulation indicated that simulated water levels contin­ run each time a change in hydraulic properties was ued to change slightly throughout the 12-month simula­ made while calibrating the transient simulation. This tion, but that these changes are, for the most part, was done in order to provide an initial potentiometric negligible (less than 1 foot). Users ofthe model should surface that was in equilibrium with the hydraulic prop­ be aware of the potential source of error when simulat­ erties that were in place at the beginning ofthe transient ing periods of many years. simulation. The steady-state simulation resulting from this iterative process is described in the following sec­ Model Calibration and Simulation tions.

Simplifications and assumptions are needed to Water levels approximate a complex three-dimensional flow system using a digital model. The discretization of hydraulic Water levels in 72 observation wells measured properties over space and surface-water changes over from mid-to late February 1985 (table 11) were used to time attenuated changes in simulated water levels and calibrate the steady-state model. The error, the differ­ flow rates that, in actuality, were large though short­ ence between the measured and simulated water levels, lived. Errors resulting from lack of knowledge about ranged from -34 feet to 24 feet. The sum of the differ­ the flow system, discretization, and simplification of ences for all 72 water levels was 4 feet. The simulated the hydraulics of the flow system for modeling can be water levels were lower than the measured or interpo­ noticed by comparing model-generated values of lated water levels in cells in the North Fork Ogden water-level altitude, water-level change, or flow rate River drainage around Eden, in an area south of the with measured values. Nevertheless, the model inte­ Middle Fork Ogden River, and in an area south of the grates the complex parts of the flow system and pro­ upper reach of the South Fork Ogden River. The simu­ vides insight into the behavior of the system under lated water levels were higher than the measured or observed and hypothetical conditions. interpolated water levels in cells in the area near Hunts­ ville. Because of the interdependence of variables involved in the ground-water-f1ow model, calibration is an iterative process whereby one hydraulic variable is Gains and losses in streams and drains revised while holding the other variables constant. Steady-state calibration was accomplished partly During calibration of the hydraulic properties, a step­ by comparing the measured and computed gains in by-step process was used to obtain acceptable values of streamflow for which data were available. Flow data water-level altitude, water-level change, and flow rate. either were obtained from Browning (1925) or are listed in table 3. The computed gains were within 50 Steady-State Calibration percent of the measured gains for nearly all the reaches. Distribution of recharge by subsurface inflow A few reaches could not be simulated reasonably from the bedrock was the first adjustment made in the by the model. The losses measured in the uppermost

71 72 Table 11. Water level in selected observation wells during shallow depths to the water table in the recharge areas, February and June 1985 and May 1986-Continued the relatively large seasonal changes in water levels, and the lack ofareally distributed historical data, a tran­ Water level, in feet below sient simulation period of about 1 year was chosen. Well or above (-) land surface location February 19-28, June 3-1, May 21-31, The simulation represented hydrologic conditions from 1985 1985 1986 February 15, 1985, to January 31,1986. The 12 stress periods represent intervals between water-level mea­ (A-7-1)35cdd-1 6.3 13.1 (A-7-1 )36bdd-1 13.1 9.4 4.6 surements, which were made about once a month at (A-7-1)36dca-1 4.5 4.5 observation wells. The climatic conditions during the (B-7-1)lbab-2 8.2 6.8 6.2 simulation period were near normal, although precipi­ (B-7-1)ldaa-1 22.2 21.9 tation during the previous water year had been much in (B-7-1)ldda-1 70.9 69.5 69.8 excess of normal.

Water-level changes in observation wells were the only reliable data available with which to calibrate reaches of the North Fork Ogden River and the South the transient simulation. Water levels in 101 observa­ Fork Ogden River and the gains measured in the lowest tion wells were measured in June 1985 and compared to reach ofthe North Fork Ogden River and at Liberty and the simulated water levels at that time. Monthly water­ Bailey Springs southwest of Liberty were not accu­ level measurements at 22 observation wells were used rately simulated because of the interaction of ground during each stress period to calibrate the transient sim­ water in the consolidated rock and the valley fill, which ulation. was not properly accounted for in the model. The sim­ ulated distribution of ground-water seepage to the indi­ During the transient simulation period, surface­ vidual channels ofSpring Creek was inaccurate, but the water data that indicated seepage to streams were avail­ total quantity of seepage to Spring Creek was closely able only for Spring Creek. Data describing seepage to simulated. Spring Creek during the snowmelt and irrigation sea­ sons could not be used to calibrate the transient model Water budget because some of the flow in Spring Creek was derived from sources other than ground-water seepage. Obser­ The steady-state water budget developed by vations of the current conditions of the river channels model simulation (table 12) was reasonably similar to were made at the same time the observation-well mea­ the water budget developed by extrapolation of the col­ surements were made. These observations were used to lected data (table 10). Although simulated flow from qualitatively adjust the model for the transient simula­ Pineview Reservoir to the confined aquifer near the tion of the ephemeral streams. Ogden well field was included in the simulated water budget, the calculated water budget did not include this In general, calibration ofthe transient simulation component of recharge. was accomplished by adjusting the hydraulic-conduc­ tivity values of the underlying aquifer and the conduc­ The steady-state water budget indicated that tance of the streambed. Some adjustment of the river about 115 cubic feet per second ofwater is recharged to stage, within reasonable limits, was made in order to and discharged from the valley-fill aquifer system. adjust the ground-water recharge from streams or the Losing streams accounted for more than one-half ofthe discharge to streams. recharge. Subsurface inflow from the consolidated rocks accounted for most of the remaining recharge. The major components of discharge are gaining Water-level changes streams, springs and drains, and Pineview Reservoir. The Ogden well field accounts for the remainder of the Simulated water-level changes in cells that repre­ simulated discharge during steady state. sent observation-well sites were compared to measured water-level changes in each observation well. The sim­ Transient Simulation ulated and measured water-level changes for selected wells are shown in figures 27 and 28. The simulated Because of the small areal extent and relatively water-level changes were similar to the measured large transmissivity ofthe valley-fill aquifer system, the water-level changes.

73 Table 12. Simulated water budget for the valley-fill aquifer system, mid-February 1985 through January 1986

[Values are in cubic feet per second, except as indicated]

Winter 1985 Mid-February Mid-March Mid-April May (steady to mid-March to mid-April to May state) (period 1) (period 2) (period 3) (period 4)

Simulated recharge

Precipitation and irrigation 0 16 119 0 76 Losing streams and irrigation distribution losses 67 80 116 142 123 Pineview Reservoir 2 2 3 12 6 Subsurface inflow 46 46 46 46 68 Total 115 144 284 200 273 Simulated discharge

Gaining streams 47 50 60 46 63 Springs and drains 28 29 39 35 42 Wells 15.1 14.5 15.5 18.5 14.2 Evapotranspiration 0 0 I 4 21 Pineview Reservoir 25 23 34 19 33 Total 115.1 116.5 149.5 122.5 173.2 Simulated change in storage, in acre-feet. (Negative values indicate decrease in storage.)

Periodic 1,600 9,800 2,500 7,900 Cumulative 1,600 11,400 13,900 21,800

An areal distribution of simulated water-level The simulated and measured discharge values are changes was compared to a map of measured water­ similar. The differences in values and trends may result level changes. The simulated water-level changes in part because the model does not simulate the storage through stress period 4, mid-February through May of ground water in the confining layer. 1985, are shown in figure 29. Overall, these simulated water-level changes (fig. 29) compare favorably with Water budget the measured water-level changes shown in figure 20. The measured water-level change map was developed The water budget determined for the transient from about 72 data points, and contours were interpo­ simulation is shown in table 12. The comparison ofthe lated where data were lacking. Some ofthe differences simulated values and the independently determined between simulated and measured water-level changes values is reasonably good. The areal recharge, subsur­ may result from interpolation of measured water-level face inflow, discharge from wells, and subsurface out­ changes where few data were available. In each ofthe flow were entered directly into the model data set. observation wells, the simulated water-level change Interchange between the aquifer and streams, drains, generally was within 50 percent of the total measured and Pineview Reservoir and discharge by evapotranspi­ water-level change during the period of the study. ration were computed by the model.

Spring Creek drainage Several discrepancies between the simulated and independently determined values can be used to yield Simulated discharge to the channels of Spring information on certain aspects of the hydrology of the Creek from layer I is shown in table 13. The approxi­ valley-fill aquifer system. More water probably mate measured discharge for the same periods (fig. 8) recharges the aquifer system from the irrigation canals also is shown. Although the data sets were compared, and ditches (particularly during July and thereafter) they were not used in calibrations. than was recognized by the seepage measurements.

74 June July August September October November December January

(period 5) (period 6) (period 7) (period 8) (period 9) (period 10) (period 11) (period 12)

Simulated recharge

68 39 38 54 36 85 13 0 66 51 49 46 73 76 76 60 5 4 3 0 0 1 2 3 91 146 87 69 46 46 46 46 230 240 177 169 155 208 137 109 Simulated discharge 40 27 19 34 42 57 52 40 34 27 24 33 35 36 36 30 14.4 14.9 15.4 10.4 9.4 13.7 13.1 12.8 75 104 82 15 4 1 0 0 39 36 50 48 46 44 35 45 202.4 208.9 190.4 140.4 136.4 151.7 136.1 127.8 Simulated change in storage, in acre-feet. (Negative values indicate decrease in storage.) 1,000 900 -1,500 1,700 1,100 2,900 100 -1,200 22,800 23,700 22,200 23,900 25,000 27,900 28,000 26,800

The independently determined values for seepage to Simulated discharge ranged from 115 to 209 cubic feet streams did not take into consideration the effects of per second. river stage on seepage. The river stage was higher dur­ ing the months ofMay through July than during steady The simulated periodic change in storage in the state. The greater river stage in the discharge areas dur­ valley-fill aquifer system (table 12) increased every ing the periods of greater flow would have decreased stress period except for periods 7 and 12. The cumula­ the rate of seepage from the aquifer system to the river. tive change from steady state through stress period 12 was nearly 27,000 acre-feet (table 12). These values The model indicated that water levels in the con­ for change in storage probably are too large and are fined part ofthe principal aquifer do not respond imme­ greater than those values calculated for February to diately to, nor as much as, the changing stage of June 1985 (see "Storage" section). The discrepancy Pineview Reservoir. During stress period 3, the stage may result because storage changes in the shallow ofPineview Reservoir rose abruptly, but water levels in water-table aquifer (layer 1) and in the principal aquifer the confined part of the principal aquifer did not north of Eden were included in the model but were not increase as much. Nearly half of the interchange of considered in the original calculations. water between Pineview Reservoir and the confined part ofthe principal aquifer was as downward seepage. Interchange between the principal aquifer and Pineview Simulation of Hypothetical Conditions Reservoir did not appear to increase substantially with the increased area of the reservoir, as was assumed The model also was used to simulate the hydro­ when discharge from Pineview Reservoir was indepen­ logic effects of two hypothetical changes in the hydro­ dently determined for May through August. logic system. The hypothetical changes were: (I) Simulated recharge for the 12 stress periods reduced recharge resulting from a drought and (2) ranged from 109 to 284 cubicfeet per second (table 12). increased discharge from wells.

75 +10 ...... A... 4" '. -l ",. '...... W . . >WI- +5 •••• •••••• Simulated w

-5 MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+10 r-T------,--,-----,,---,----,---r-----,----.---r------,---,--,

oj 4 ...... ••. > WI- 0 ....~..-. '. w

-20 L....L__--'-_----J'---_--'-__.1--_---'-__--I.-_----J'---_--l....__-'---_--'-__--'----' MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+5 '"

-l ...... W >WI- w

Figure 27. Simulated and measured water-level change for three observation wells in the upper North Fork Ogden River valley, 1985-86.

76 +20 r-r----.------,-----.------,-----.------,--,------.--,------.----,--, ...... ' ..... +10 ~....._-...... "'\'" Measured .... \ ••••• Simulated ...... '. \ .. ' (A-6-2)15acb-1 ...'" ...... •• , .AI'"

-10 L-.J...__--'---_----JL.-_--'--__-'--_--'-__--'---_----JL.-_--'--__-'--_--'-__--'-----' MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+15

....J LlJ +10 >LlJ-1- LlJ(9LlJ -,lZLlJ 1l:«Ll.. +5 LlJIZ 1-;0- ~ 0

-5 MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+40

....J +30 LlJ >WI- LlJC)LlJ +20 -,lZLlJ .It.,.",... 1l:«Ll.. ••••••• Simu\ed LlJIZ +10 ~ ~ _ ~ 1-;0- .:.' ...... ~ * ...... - 0 (A-6-1)11cab-1 -10 MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

Figure 28. Simulated and measured water-level change for three observation wells in the south part of Ogden Valley, 1985-86.

77 EXPlANATION Water-level change, in feet

-5 to 5

111°52'30' 5 to 10 I • 10 to 15

·0":::••••...: •rIIlJIIlIj::::::::. 15 to 20 Greater than 20 •CJ Inactive cell Negative values indicate declines; Positive values indicate rises

R.1W.

41°15'-

Base from U.S. Geological Survey Ogden, 1:100,000,1976

o 2 3 MILES I I I I a 2 3 KILOMETERS R.1 E.

Figure 29. Simulated water-level change in the principal aquifer, mid-February through May 1985.

78 Table 13. Simulated and measured discharge to Spring Creek

Simulated discharge Measured discharge Stress period Monthly period (cubic feet per second) (cubic feet per second)

I Mid-February to mid-March 10.8 II 2 Mid-March to mid-April 15.4 17 3 Mid-April to May 15.5 12 4 May 21.4 15 5 June 16.6 20 6 July 10.7 16 7 August 9.0 II 8 September 11.1 8 9 October 12.3 7 10 November 12.6 7 11 December 12.4 8 12 January 12.0 9 Mean discharge 13.3 11.8

Drought increases occurred during stress periods 2 (mid-March to mid-April) and 10 (November). Considerably less Ogden Valley has experienced several droughts, water was exchanged between the confined part of the but little information is available on the hydrologic principal aquifer and Pineview Reservoir during the effects ofdrought over a wide area ofthe valley. There­ simulated drought period. Recharge from streamflow fore, computer simulation of a drought year, with con­ diminished, most likely because fewer stream reaches ditions si milar to those during 1977, was made with the were active in the recharge areas, and the river stages hydraulic properties used in the transient calibration. were not as high. During the simulated drought, total Fewer active river reaches in the recharge area, lower recharge varied from 113 to 204 cubic feet per second, river stages, lower Pineview Reservoir stages, less and total discharge varied from 103 to 173 cubic feet recharge from bedrock, and lower rates of areal per second. recharge from precipitation and irrigation were included in the model data based on probable condi­ tions. Data collected in 1977 were used to help concep­ Increased Discharge from Wells tualize the probable conditions. Withdrawals from three additional wells, each The water budget and water levels for the 1985­ discharging at a rate of I cubic foot per second, also 86 simulation period were compared to the water bud­ were simulated. The simulated wells were located get and water levels of the simulated drought period to northwest of Liberty, northwest of Eden, and east of observe water-level declines and storage changes. Huntsville. All three wells derived their water from Water levels for the simulated drought period were layer 2; the Eden and Huntsville wells were in the con­ lower than those for the 1985-86 simulation period and fined part of the principal aquifer, and the Liberty well did not show as much seasonal fluctuation (fig. 30). was in the unconfined part of the principal aquifer. Water levels near Pineview Reservoir and in the South Fork Ogden River drainage east of Huntsville showed The simulation of additional discharge and the original 1985-86 simulation were compared using the the greatest declines from 1985-86 levels. The greatest water levels in observation wells, the storage changes, declines for the simulated drought occurred during the and the overall water budget. The water levels in obser­ spring and early summer months. vation wells did not change noticeably, indicating that Water budgets for the 1985-86 simulation period very little of the additional water came from storage in and the simulated drought period showed some sub­ the aquifer. The rate of increase in storage in the aqui­ stantial differences. Overall storage losses during the fer declined by about I cubic foot per second during simulated drought occurred during stress periods 5 stress periods 5 through 8, as indicated by the water through 7 (June-August). The most substantial storage budget.

79 +30

....J LU +20 > LU"I- 1985-86 LU(!)LU a:«LL-,lZLU +10 / LUIZ ...... '...... 'lI!It... Drought 1-:0- ,".' ...... '."',16., / ~ 0 ••••••• • •••• 4r ~ (A-6-1)11cab-1 ··-· ·A········... -10 MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+20

....J LU +10 >WI- LU(!)LU -,lZLU 0 +-----4...... Drought a:«LL ...... "., / LUIZ 1-:0- ••••••6-. A -10 ...... ' a ~ (A-6-2)15acb-1 _. 'A"" - .A·····

-20 MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

+10 r------,

....J LU . > LU" I- 0 4---*"-' ... LU (!) LU •••• -,lZLU ...... ffi ~ ~ 6- Drought I-:()- -10 •••••• ..\. / ~ . ·······.A ······.\ (A-7-1)7dba-1 -20 L-L__---'-__L.-_-"-__-'--_---'-__---'-__L.-_-"-__-'-----_---'-__-'---' MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN 1985 I 1986

Figure 30. Water·level change in wells in Ogden Valley for 1985-86 simulation and for drought simulation.

80 The two water budgets were compared for each vation wells. In the model, some wells were in the same stress period even though the total quantity ofchange in cell as a river reach. When the river reach went dry, the water budget during each stress period could not water levels in wells from these river cells declined exceed the total additional well discharge of 3 cubic more than could be expected realistically. The use of a feet per second. Evapotranspiration was slightly more detailed grid in a finite-difference model or a affected. Reduced seepage to Pineview Reservoir dur­ finite-element model probably would minimize this ing the later stress periods probably was caused by problem. pumping of the simulated Eden well. Pumping of the simulated Huntsville well appeared to divert water that SUMMARY AND CONCLUSIONS would have discharged to Spring Creek and to drains in the immediate area. Pumpage of the simulated Liberty The area surrounding Ogden Val1ey is consoli­ and Eden wel1s caused reduced ground-water storage dated rock. The consolidated rocks that transmit and and reduced discharge to streams. The simulated Lib­ yield the most water in the area are the carbonate rocks erty well likely induces streamflow from the North Fork and the Wasatch Formation. Infiltration of snowmelt, Ogden River channel to recharge the aquifer; the simu­ mostly on the widespread Wasatch Formation, is the lated Eden well probably intercepts water that normally predominant source of recharge. Discharge from con­ discharges to the North Fork Ogden River channel. solidated rocks is by streams, evapotranspiration, springs, subsurface outflow, and wells. NEED FOR FURTHER REFINEMENT OF The unconsolidated valley-fill deposits in Ogden THE COMPUTER SIMULATION Valley are more than 750 feet thick and comprise the valley-fill aquifer system. The valley-fill aquifer sys­ The computer simulation presented in this report tem includes a principal aquifer with confined and accomplished the purpose of estimating the probable unconfined parts and a shallow water-table aquifer that range in values and distribution of hydraulic properties overlies the confined part ofthe principal aquifer and is and provided an estimate of the rates of the various separated from it by a silty clay layer. recharge and discharge components of the aquifer sys­ Ground-water movement in the valley-fill aquifer tem. The available data are not adequate to accurately simulate ground-water flow in the hydrologic system system is from the area along the margins of the valley over a lengthy period of time and for changing hydro­ toward Pineview Reservoir in the southern part of the logic conditions. val1ey. The vertical head gradients are downward in the recharge areas and upward in the discharge areas. The ground-water-f1ow model could not accu­ Upward movement of water occurs from the confined rately define the surface-water influence on the ground­ part of the principal aquifer through the confining bed water system. More data on surface-water conditions to Pineview Reservoir and Spring Creek. are needed. Better definition ofriver and drain seepage, improved timing and location ofdry reaches in the river A water budget for the valley-fill aquifer system channels, and a better definition of the distribution and was estimated for mid-February 1985 through January rate of leakage to Pineview Reservoir are needed. 1986. Because of the substantial seasonal variation in hydrologic conditions resulting from climatic varia­ The observation-wel1 network established for tions, the budget presented is unique for that time this study was adequate for the monthly observations of period. In general, the water-budget indicates that the most substantial water-level changes but not for several majority of recharge is from irrigation, losing streams, areas ofprobable large water-level changes. Therefore, and subsurface inflow. Precipitation and irrigation dis­ additional observation wells are needed in many areas, tribution losses are relatively minor contributors to such as near Liberty. recharge. Discharge is to streams, springs, drains, Subsurface inflow, probably one of the largest wells, evapotranspiration, and Pineview Reservoir. contributors of recharge to the ground-water system, The range and distribution of hydraulic proper­ was not and probably cannot be measured. Better defi­ ties were clarified using a combination of field and lab­ nition of the distribution of recharge, particularly the oratory data. An aquifer test completed for this study seasonal change in rate, is needed. indicated that a transmissivity value of about 79,000 The discretization of streams into cells led to feet squared per day was the most representative value problems with calibration using water levels in obser- for the confined part of the principal aquifer. Hydrau-

81 lie-conductivity values from laboratory tests were less REFERENCES CITED than 0.013 foot per day for the confining layer. Vertical Avery, Charles, 1986, Bedrock aquifers of eastern San hydraulic conductivity of the confining layer ranged Juan County, Utah: Utah Department of Natu­ from 0.0 I to 0.04 foot per day according to reservoir­ ral Resources Technical Publication No. 86, bed seepage measurements. 114 p. Water in the valley-fill aquifer system has a dis­ ---1987, Chemistry of thermal-water and esti­ solved-solids concentration that does not exceed 350 mated reservoir temperatures in southeastern Idaho, north-central Utah, and southwestern milligrams per liter, and most of the water is a calcium Wyoming: 1987 Wyoming Geological Associ­ bicarbonate type. The water is slightly more mineral­ ation Guidebook, p. 347-353. ized in the Middle Fork Ogden River and South Fork Browning, H.W., 1925, Report on a hydrographic sur­ Ogden River valleys. Relative to the general water vey of the Ogden River system during the qual ity in the valley, nitrate, pH, and water temperature irrigation season of 1925: Unpublished manu­ were slightly anomalous in localized areas. script on file in offices of the U.S. Geological Survey and the Utah State Engineer. A three-dimensional, finite-difference computer Bureau of the Census, 1982, 1980 Census of popula­ model was used to simulate ground-water flow in the tion, number of inhabitants, Utah: U.S. valley-fill aquifer system and thus, enable a better Department ofCommerce, v. I, chap. A, pt. 46, understanding ofthe system. Two hypothetical changes 30 p. in the aquifer system, a I-year drought and withdrawals Crittenden, M.D., Jr., 1972, Geologic map of the from 3 additional wells, were simulated to estimate the Browns Hole quadrangle, Weber County, effects of these changes on streamflow and ground­ Utah: U.S. Geological Survey Geologic Quad­ water levels. rangle Map 968, scale I:24,000, I sheet. Crittenden, M.D., Jr., and Sorensen, M.C., 1985a, Geo­ Drought conditions similar to those during 1977 logic map ofthe Mantua quadrangle and part of were simulated to estimate the hydrologic effects of the Willard quadrangle, Box Elder, Weber, and drought on Ogden Valley. Water levels in the principal Cache Counties, Utah: U.S. Geological Survey aquifer were lower for the simulated drought period Miscellaneous Investigations Series 1-1605, than for the 1985-86 simulation period and did not scale I:24,000, I sheet. show as much seasonal fluctuation. Interchange of ---I985b, Geologic map of the North Ogden quad­ water between the confined part ofthe principal aquifer rangle and part of the Ogden and Plain City and Pineview Reservoir during the simulated drought quadrangles, Box Elder and Weber Counties, period was reduced. Utah: U.S. Geological Survey Miscellaneous Investigations Series 1-1606, scale I:24,000, I Withdrawals from three additional wells also sheet. were simulated, and water levels in observation wells Davis, FD., 1985, Geology of the northern Wasatch did not change noticeably, indicating very little addi­ Front: Utah Geological and Mineral Survey tional water came from storage. Reduced seepage to Map 53-A, scale I: 100,000, 2 sheets. Pineview Reservoir and reduced discharge to streams Doyuran, Vedat, 1972, Geology and ground-water also were noted. resources ofOgden Valley, Utah: Unpublished Ph.D. thesis, University of Utah, 134 p. In order to simulate ground-water flow for vary­ Duthie, J.R., 1972, Detergent developments and their ing hydrologic conditions, more data need to be col­ impact on water quality, in Allen, H.E., and lected on surface-water conditions. More wells are Kramer, J.R., eds., Nutrients in natural water: needed in several areas in orderto add control points for New York, John Wiley and Sons, Inc., 457 p. water-level measurements. Additional observation Eardley, A.J., 1944, Geology of the north-central wells in the Liberty area, in particular, would provide Wasatch Mountains, Utah: Geological Society useful control data. of America Bulletin, v. 55, p. 819-894.

82 Farnsworth, RK., Thompson, E.S., and Peck, E.L., Messer, U., Slezak, Lloyd, and Liff, c.1., 1982, Poten­ 1982, Evaporation atlas for the contiguous 48 tial for acid snowmelt in the Wasatch United States: National Oceanic and Atmo­ Mountains: Water Quality Series UWRLlQ­ spheric Administration, National Weather 82/06, Utah Water Research Laboratory, Utah Service Technical Report 33, 26 p. State University, 37 p. Fenneman, N.M., 1931, Physiography of the western Mullens, T.E., 1969, Geologic map ofthe Causey Dam United States: New York, McGraw-Hill, Quadrangle, Weber County, Utah: U.S. Geo­ 534 p. logical Survey Geologic Quadrangle Map 790, scale 1:24,000, 1 sheet. Feth, J.H., Barker, D.A., Moore, L.G., Brown, R.I., and Veirs, C.E., 1966, Lake Bonneville: Geology Sorensen, M.e., and Crittenden, M.D., Jr., 1979, Geo­ and hydrology of the Weber Delta District, logic map ofthe Huntsville quadrangle, Weber including Ogden, Utah: U.S. Geological Sur­ County, Utah: U.S. Geological Survey Geo­ vey Professional Paper 518, 76 p. logic Quadrangle Map 1503, scale 1:24,000, 1 sheet. Fortier, Samuel, 1897, Preliminary report on seepage water and the underflow of rivers: Utah Agri­ Stewart, S.W., 1958, Gravity survey of Ogden Valley cultural College Experimental Station Bulletin in the Wasatch Mountains, north-central Utah: 38,35 p. Transactions of the American Geophysical Union, v. 39, No.6, p. 1151-1157. Haws, F.W., Jeppson, RW., Huber, A.L., 1970, Hydro­ logic inventory of the Weber River study unit: Stiff, H.A., Jr., 1951, The interpretation of chemical Utah Water Research Laboratory Report PR­ water analysis by means ofpatterns: Journal of WG40-6, Utah State University, 131 p. Petroleum Technology, v. 3, No. 10, p. 15-17. Herbert, L.R, Croff, RW., Clark, D.W., and Avery, Stokes, W.L., ed., 1963, Geologic map of Utah: Uni­ Charles, 1987, Seepage studies of the Weber versity of Utah, scale 1:250,000, 4 sheets. River and the Davis-Weber and Ogden Valley Thomas, RE., 1945, The Ogden Valley artesian reser­ Canals, Davis and Weber Counties, Utah, voir, Weber County, Utah: Utah Department 1985: Utah Department of Natural Resources of Natural Resources Technical Publication Technical Publication No. 90, 53 p. No.2, 37 p. Lee, D.R, 1977, A device for measuring seepage flux ---1952, Ogden Valley, Weber County, in Tho­ in lakes and estuaries: Limnology and Ocean­ mas, H.E., Nelson, W.B., Lofgren, B.E. and ography, v. 22, No.1, p. 140-147. Butler, RG., eds., Status of development of Leggette, RM., and Taylor, G.H., 1937, Geology and selected ground-water basins in Utah: Utah ground-water resources of Ogden Valley, Department of Natural Resources Technical Utah: U.S. Geological Survey Water-Supply Publication No.7, p. 88-96. Paper 796-D, p. D99-D161. ---1963, A water budget for the artesian aquifer in Lofgren, B.E., 1955, Resume of the Tertiary and Qua­ Ogden Valley, Weber County, Utah, in Ben­ ternary stratigraphy of Ogden Valley, Utah, in tall, Ray, compiler, Methods of collecting and Eardley, A.I., ed., Tertiary and Quaternary interpreting ground-water data: U.S. Geologi­ geology ofthe eastern Bonneville Basin: Utah cal Survey Water-Supply Paper 1544-H, p. Geological Society Guidebook No. 10, H63-H97. p.70-84. Thompson, K.R., 1983, Reconnaissance of the quality Lohman, S.W., 1972, Ground-water hydraulics: U.S. of surface water in the Weber River basin, Geological Survey Professional Paper 708, Utah: Utah Department of Natural Resources 70 p. Technical Publication No. 76, 74 p. McDonald, M.G., and Harbaugh, A.W., 1984, A mod­ U.S. Environmental Protection Agency, 1986, Quality ular three-dimensional finite-difference criteria for water 1986: Office of Water, Reg­ ground-water flow model: U.S. Geological ulations and Standards, U.S. Environmental Survey Open-File Report 83-875, 528 p. Protection Agency.

83 u.s. National Oceanic and Atmospheric Administra­ tion, 1982, Monthly normals of temperature, precipitation, and heating and cooling degree days 1951-80, Utah: U.S. National Oceanic and Atmospheric Administration Climatogra­ phy of the United States No. 81 (Utah), 14 p. U.S. Weather Bureau, 1963, Normal annual and May­ Septemberprecipitation (1931-60) for the State of Utah: Map of Utah, scale 1:500,000, 1 sheet.

84 ~~~It! ~UTAH

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